11th ICRS Abstract book - Nova Southeastern University

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1-17 Holocene Reef Development At The Flower Garden Banks: Recent Surprises William PRECHT* 1 , Ken DESLARZES 2 , Emma HICKERSON 3 , G.P. SCHMAHL 3 , James SINCLAIR 4 , Richard ARONSON 5 1 Applied Coastal and Environmental Services, Battelle Memorial Institute, Miami Lakes, FL, 2 Marine Sciences, Geo-Marine Inc., Plano, TX, 3 Flower Garden Banks National Marine Sanctuary, NOAA, Galveston, TX, 4 Gulf of Mexico Region, Minerals Management Service, New Orleans, LA, 5 Marine Sciences, Dauphin Island Sea Lab, Dauphin Island, AL The first living colonies of Acropora palmata were discovered on the Flower Garden Banks (FGB) in 2003 and 2005. Those discoveries, coupled with a known history of bank flooding since the last glacial maximum, led us to predict that Acropora-dominated reefs underlie and form the structural foundation of the living reef community at the FGB. In June 2006, while scuba diving on the southeast corner of the East FGB, we examined an open cave at 21 m depth, which exposed a 3-m vertical section of the reef subsurface just below the living community. Within that exposure we discovered large branches and trunks of A. palmata (>1 m in height) in growth position. Radiocarbon dating of a branch from a colony at the top of the section yielded a date of 6330 ± 60 14Cyr (radiocarbon years before 1950), corresponding to a calibrated age of 6780 calbp. Follow-up surveys in June 2007 revealed an A. palmata dominated under story dating between 10-6 ky on both banks. The discovery of fossil A. palmata has profound implications for understanding the history of reef development at the FGB. The banks supported a shallow, warm-water, reef-coral assemblage up until ~6000 years ago. This community lagged behind rapidly rising sea level in the middle Holocene. As sea temperatures cooled in the late Holocene the reef was capped by a eurythermal deeperwater assemblage dominated by massive corals, which persists to this day. During our 2007 surveys we also found the first fossils of Acropora cervicornis on the East FGB. This species appears to have persisted (and flourished) until the Little Ice Age in deeper water on the flanks of the Bank. Follow-up studies are proposed to document and explain the turn-on and turn-off mechanisms for Acropora reef development on these isolated reef complexes. 1-18 Response Of acropora To Warm Climates; Lessons From The Geological Past Clare WHITE* 1,2 , Brian ROSEN 3 , Dan BOSENCE 1 1 Earth Sciences, Royal Holloway University of London, Egham, Surrey, United Kingdom, 2 Palaeontology, Natural History Museum, London, United Kingdom, 3 Zoology, Natural History Museum, London, United Kingdom Predictions about the future responses of modern coral reefs to global climatic change lack data from the deeper past. The geological record offers a storehouse of information which documents how reef coral palaeodistributions have been highly sensitive to climate change, modulated by the availability of suitable habitats. The geological record of one individual taxon, Acropora, illustrates how an important reef coral genus has responded to climate change, and additionally tectonics, through its Cenozoic history. We have reconstructed Acropora’s changing spatio-temporal distribution using museum specimens, literature reviews and databases, and plotted the data on a time-series of palaeogeographic maps and on ‘Boucotgrams’. Unlike Acropora’s widespread lowlatitude distribution today, with its centre of diversity in the Indo-West Pacific, this coral was absent from this region in the Paleogene to early Neogene, but was common in Europe. Here we highlight (1) latitudinal changes in distribution in response to major climatic trends, and (2) the relatively late arrival of Acropora in the Indo-West Pacific, apparently in response to tectonically-driven rearrangement of Tethyan and Indo-Pacific seaways and land-masses around the end of the Paleogene. Focusing on a particular section of this record, the high palaeolatitude (48˚N) occurrences in the Middle-Late Eocene (~48-33Ma) of southern England and northern France, we use taphonomic and geochemical analyses to reconstruct the palaeoenvironmental setting. This confirms that Acropora existed in tropical-like climatic conditions in Northwest Europe during the Eocene. This individual coral genus’s latitudinal expansion, compared with modern distributions, illustrates “coral creep” as a response to the hot greenhouse setting of the early Cenozoic, and periods of extreme climatic warming of the Eocene, with sea-surface temperatures and ρCO2 higher than present. Hence this work shows how the geological record can provide information to complement predictions on the fate of modern coral reef genera with respect to climate change. Oral Mini-Symposium 1: Lessons From the Past 1-19 Abrupt Drowning And Cooling 8.2-8.4 Ka Observed In A 0.8-M Diameter And 24-M Long Core Through A Hawaiian Coral Reef, Oahu, USA Eric GROSSMAN* 1 , Jody WEBSTER 2 , Christina RAVELO 3 , Jim BARRY 4 , Stewart FALLON 5 , Yael SAGY 1 , Bruce RICHMOND 1 , Mike TORRESAN 6 , David CLAGUE 7 1 Coastal and Marine Geology Program, US Geological Survey, Santa Cruz, CA, 2 School of Earth and Environmental Sciences, James Cook University, Townsville, Australia, 3 Ocean Sciences Department, University of California, Santa Cruz, Santa Cruz, CA, 4 Sea Engineering, Inc., Honolulu, HI, 5 Research School of Earth Sciences, Australian National University, Canberra, Australia, 6 Coastal and Marine Geology Program, US Geological Survey, Menlo Park, CA, 7 Monterey Bay Aquarium Research Institute, Moss Landing, CA Sediment collected in a 0.8 m diameter, 24 m long core at 18 m depth offshore of Pearl Harbor provide a geologic archive of reef response to the Holocene sea-level transgression on the island of Oahu, Hawaii. CHIRP seismic reflection data reveal a 5-15 m thick reef complex buried below the seafloor within a paleostream valley. An olivine-rich, black sand and rounded basalt cobble unit, inferred as an early Holocene delta occurs at the base of the core overlying a soilstained, caliche-encrusted limestone dated to 124 ka. 14-C ages indicate a shallow-water coral reef assemblage comprised of encrusting P. lobata and branching coralline algae P. gardineri accreted until 8.4 ka, then was abruptly replaced by a mono-specific P. compressa reef between 8.4 and 8.2 ka and added 10 m to the reef by about 4.9 ka. Approximately, 4.5 m of carbonaterich sand buried this reef complex and comprises the modern seafloor substrate at the site. The abrupt transition from shallow-water to deeper-water coral assemblages at 8.4-8.2 ka is coincident with rapid climate change observed in other reefs, lakes, and sedimentary records throughout the tropics. Reconstruction of paleowater depths at this transition indicates a rapid rise in sea level of at least 3 m, helping to explain preservation of a drowned erosional notch surrounding many shorelines of Hawaii at -24 m like a bath-tub ring. High-resolution measurements of δ18O and Sr/Ca ratios from three P. compressa corals 8.7-8.3 ka, indicate cooler surface water temperatures than today and a slight cooling during this event. Abrupt sealevel rise of several meters could explain the transition in coral community structure, the dominance of mono-specific P. compressa, and colder sea surface temperatures. 1-20 Evidence of rapid sea-level rise from reef backstepping during the Last Interglacial highstand. Paul BLANCHON* 1 1 Inst. of Marine Sciences & Limnology, National University of Mexico, Cancun, Mexico Investigation of reef development during the Last Interglaciation has focussed on flights of exhumed terraces in neotectonic terranes. But the timing of climatic cycles has taken precedence over reef response to sea-level change. As a result, we have no clear picture of highstand reef development nor sea-level changes that controlled it. Here I report the facies architecture of a highstand reef from the NE Yucatan Peninsula that affords significant insight into reef development and sea-level behaviour during the Last Interglaciation. Excavations for a theme park (Xcaret) have exposed two coeval reef-tracts that are offset and at different elevations. The lower-tract crops-out along the coast and the crest facies reaches an elevation of +3.0 m amsl. One hundred metres in-land, the crest of the uppertract reaches +5.7 m amsl. Crests in both tracts were true breakwaters, each consisting of large colonies of A. palmata and boulder-sized fragments with a suite of surf-zone encrusters. Lowertract frameworks are occluded by crustose corallines, but those in the upper-tract remained open and were infiltrated by abraded sand during forced shoreface regression. This infiltration is clear evidence that the upper-tract was younger than the lower, and that reef backstepping occurred. Backstepping was not related to shelf flooding to the north, because that had occurred during lower-tract development. But backstepping was accompanied by increased sediment flux that shifted lagoonal biofacies to a sediment-tolerant assemblage. Similar changes occurred in the strand-plain sequence to the north, but here it involved a switch from low- to high-energy coastal sedimentation. This energy switch and reef backstepping are both consistent with a +3 m sea-level jump at the end of the Last-Interglacial highstand. 5
1-21 Coral Reef Development Along The Windward Platform Margin Since The Plio- Pleistocene: Southern Exuma Cays, Bahamas (Dedicated To Robert F. Dill, 1927- 2004) Paul J. HEARTY* 1 , Donald F. MCNEILL 2 1 GeoQuEST Research Centre, School of Earth and Environmental Sciences, University of Wollongong, Australia (paulh@uow.edu.au), Wollongong, NSW, Australia, 2 MGG- RSMAS, University of Miami, Miami, FL The surface geology and two 33-m cores from the Exmas contain 11 limestone-paleosol “couplets” (C1 to C11 – older to younger), revealing depositional cycles extending back to the Plio-Pleistocene. The couplets are composed of marine limestone and terra rossa paleosol-karst exposure surfaces. Amino acid racemization and paleomagnetic reversals provide a functional chronostratigraphy for the couplets. At the base of the more bankward Core #2, couplets C1 to C3 contain the coral Stylophora, generally associated with the Plio-Pleistocene. The overlying C4 complex consists of several meters of dense reddish paleosols and thin intertidal lenses. These C4 paleosols bracket the Brunhes- Matayuma boundary (0.78 Ma; MIS 19?), and collectively equate with the “Big Red Soil” recognized on Bermuda and Hawaii. This interval comprises a succession of much lower highstands reflecting more interglacial continental ice from 0.5-1.0 Ma. Younger units C5 through C11 were deposited 0.5 Ma to present, and record lesser-known middle Pleistocene sea levels (MIS 15 @ -15 m, MIS 13 @ -7 m, and MIS 7 @ -18 m). In contrast, important interglacials during MIS 11 and 9 left little sedimentary evidence, probably due to deep flooding of the platform, and the dearth of early Pleistocene antecedent topography on which to “hang” deposits. Sea-level cycles across the Plio-Pleistocene show a general progression from reefal components to predominantly non-skeletal sands. Plio-Pleistocene highstands (3.0? - 1.0 Ma) are obscured below present sea level by subsidence. Corals are a key component of units C2, C3, C4 in Core #2 and unit C6 in the more seaward Core #1. A long period of subaerial exposure from 1.0-0.5 Ma was followed by several important mid to late Pleistocene highstand carbonate accretionary events during which the platform margin extended to its present position over 3 km eastward. 1-22 Mid-Brunhes First High Amplitude Transgression(s): Platform Top and Siliciclastic Shelf Contemporaneous Re-flooding Recorded on the Slopes of Great Bahama Bank and Central Belize Barrier Reef Andre DROXLER* 1 , Brooke E. CARSON 2 1 Earth Science, Rice University, Houston, TX, 2 Shallow Marine Stratigraphy Team, Chevron Energy Technology Company, Houston, TX Last 5 My ice volume variations recorded in stacked, globally distributed, benthic oxygen records, clearly show a systematic late Pliocene and early Pleistocene ice volume increase following an early Pliocene sea level highstand estimated to be 15 to 25 m higher than current sea level. This systematic ocean base-level fall was terminated by two mid Brunhes high amplitude transgressions at the MIS 16-15 and MIS 12-11 glacial to interglacial deglaciations. On the slopes of Great Bahama Bank (GBB) and central Belize Barrier Reef (BBR), a series of five-six stacked and contemporaneous highstand wedges are observed and identified as being linked to the MIS 15-13, 11, 9, 7, 5, and 1 interglacial stages. Each package is defined by high concentration and/or mass accumulation rates of bank derived fine aragonite sediment bounded by intervening late glacial intervals enriched in Mg calcite cement corresponding to marine hardgrounds on the western margin of GBB and intraclasts-rich levels with coarser grain concentrations on the slope off the BBR. The highstand wedges are overlying an interval in both areas with lower bank-derived aragonite concentration and/or mass accumulation rates, higher pelagic calcite concentrations, and overall lower sedimentation rates. Based upon these observations, the two mid-Brunhes major MIS 16-15 and MIS 12-11transgressions correspond to first a partial and then a full re-flooding of GBB top and the siliciclastic fluvial plain established at lower base level during the late Pliocene and early Pleistocene sea level regression in Belize. These two mid-Brunhes transgressions have most likely triggered also the onset of modern barrier reefs along the Queensland and New Caledonia margins, the Florida Keys, and globally modern atolls. The MIS 12-11 transgression marks the first time interglacial atmospheric CO2 concentrations reached late Brunhes values between 280-295 ppm which has been suggested to be related to the global neritic carbonate re-establishment. Oral Mini-Symposium 1: Lessons From the Past 1-23 Late Miocene To Recent Coral Community Dynamics in The Gulf Of California Ramón LÓPEZ-PÉREZ* 1 1 Instituto de Recursos, Universidad del Mar, Puerto Angel, Mexico Hermatypic coral studies in the Gulf of California have focused mainly on the distribution, abundance, ecology, and biogeography of modern species, but relatively few of these works have studied fossil corals. Miocene to Pleistocene coral communities in the Gulf of California were targeted in order to assemble a detailed geologic and taxonomic framework for already known and new coral bearing units. In general, coral bearing units are small and represent single spatio-temporal growth episodes ranging in age between late Miocene to late Pleistocene. Identification of recently collected specimens reveals that previously recognized coral species probably represent ~ 50 % of the Gulf of California fauna. Cluster analysis, multidimensional scaling and analysis of similarity of presence/absence and relative abundance data demonstrated that Gulf of California coral reef assemblages experienced larger temporal differences in species composition and relative abundance than expected by chance. Coral species originated and were added to the species pool during late Miocene-early Pliocene and Pleistocene. Gulf of California assemblages consisted of locally originated Caribbean-like species between late Miocene and late Pliocene when extinction peaked at the Plio-Pleistocene transition. During the Pliocene assemblages consisted of a mix of extinct and living species co-occurring within and among localities, but immediately after the demise of pre-turnover taxa, living Indo-Pacific immigrant species dramatically increase in number and relative abundance ruling out ecological replacement as the key factor in pre-turnover species extinction. The turnover is unique in that pre-turnover species origination resulted from the formation of the Gulf of California, and instead of reducing species richness, the extinction event triggered the long-distance colonization of species. More data and better resolved age dates are necessary to understand the cause of faunal turnover, and the relative importance of biological and environmental factors in the faunal change. 1-24 Caribbean Coral Reef Types From A Mixed Siliciclastic-Carbonate Setting: Miocene- Pliocene Of The Dominican Republic Donald MCNEILL* 1 , James KLAUS 2 , Ann BUDD 3 1 Marine Geology & Geophysics, Rosenstiel School - University of Miami, Miami, FL, 2 Department of Geological Sciences, University of Miami, Coral Gables, FL, 3 Department of Geoscience, University of Iowa, Iowa City, IA Geologic models of ancient Caribbean coral reefs that occur in predominantly siliciclastic settings have developed and diversified since the 3rd Coral Reef Symposium in 1977. The objective of this study is to characterize the styles of reef development in these mixed siliciclastic-carbonate settings from the exceptionally well-preserved fossil reef deposits in the Cibao Basin, northern Dominican Republic. Building on the mixing classification of Mount (1984), we recognize three main styles (geometries) of "in situ" carbonate (reef) deposition within siliciclastics. These include: 1) late Miocene stacked patch reefs-these reefs occur as isolated patches approximately 20-30 m thick and 300-400 m wide as part of a shallow clinoformal shelf. Lowered sea level and initial transgression provided conditions favorable to patch reef initiation and development; 2) late Miocene-early Pliocene bedded coral in mudthese reefs occur as either thick beds (3-6 m thick) of mud with abundant coral and coral fragments scattered throughout, or as distinct, cyclic coral beds (0.5-1 m thick) interbedded with mud beds (
Page 2 and 3: Contents Sponsors..................
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Page 12 and 13: Plenary Lessons from the Past Malco
Page 14: Plenary Drivers of Coral Infectious
Page 18 and 19: 1-1 The R/v Alpha Helix Symbios Exp
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7-37 Developing An Expert System Fo
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7-45 The Effect Of Sediment And Hea
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8-1 From Bacterial Bleaching To The
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8-9 Milkfish Feces Share Common Bac
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8-17 Bacteria Associated With Symbi
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8-26 Photosynthetic Microorganisms
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8-35 Tissue Loss And Tropical Storm
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9-5 Evaluation Of Biotic And Abioti
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9-13 Is Allelopathy Involved in Cor
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Oral Mini-Symposium 10: Ecological
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10-41 Substrate Effects On Reef Fis
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12-5 The Contribution Of Heterotrop
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12-14 Ocean Dynamics Drive Coral Re
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12-23 Coral Reef Resilience To Chro
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13-1 Prioritizing Conservation Hots
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Oral Mini-Symposium 13: Evolution a
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14-6 Modelling Coral Larval Dispers
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14-14 Environmentally-Mediated Vari
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14-21 Same, Same, But Different: Co
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14-29 Complex Patterns of Genetic C
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14-37 Genetic Connectivity in Phili
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14-45 Range-Wide Population Genetic
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14-55 The Importance Of Behavior On
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Oral Mini-Symposium 15: Progress in
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Oral Mini-Symposium 15: Progress in
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Oral Mini-Symposium 16: Ecosystem A
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Oral Mini-Symposium 17: Emerging Te
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18-5 Coral Reef Habitat Around New
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18-13 Response Of High Latitude Her
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18-21 Socio-Economic Monitoring (So
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18-29 Extent And Timing Of Disturba
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18-37 It Depends On Where You Look:
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18-45 New Insights Into The Exposur
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Oral Mini-Symposium 19: Biogeochemi
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Oral Mini-Symposium 20: Modeling Co
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Oral Mini-Symposium 20: Modeling Co
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21-9 Integrated Economic Valuation
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21-19 Towards Local Fishers Partici
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21-27 The Political Aspects Of Resi
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21-37 Exploitation And Trade Of Cor
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22-1 Complex Ecological Effects Of
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22-9 Comparative Evaluation Of Reef
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22-17 Managing Fishing Gear To Enco
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22-25 Estimating Harvest Pressure O
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22-33 Are The Coral Reef Finfish Fi
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22-41 Using Length-Frequency Data T
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22-50 Changes in Ecosystem Structur
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23-5 Measuring Success in Managing
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23-13 Some Hints About The Impacts
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23-21 Fishery Management For Artisa
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23-29 “To Live With The Sea”; D
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23-37 Challenges Facing An Mpa Mana
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23-45 Assessing Global Coral Reef M
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23-53 Developing A Model For Ecosys
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23-61 Mitigating The Effects Of Cor
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23-69 Restore Or Not To Restore? Vl
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24-1 Fates Of Restored Acropora Pal
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24-9 Sponge-Mediated Coral Reef Res
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24-17 Coral Community Restorations
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24-25 Development Of A Coral Nurser
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24-33 Transplantation of Porites lu
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24-41 Scleractinian Coral Relocatio
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24-50 Gametogenesis in Cultured Ver
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Oral Mini-Symposium 25: Predicting
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Oral Mini-Symposium 26: Biodiversit
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26-54 Gene Genealogies Reveal Phylo
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Poster Session
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1.13 Depth-Related Patterns of Infa
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1.20 Grain Size And Sedimentary Con
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1.3 Environmental Effects On Back-R
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Poster Mini-Symposium 2: Biotic Res
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Poster Mini-Symposium 3: Calcificat
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Poster Mini-Symposium 4: Coral Reef
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7.162 Disease Ecology And Local Pat
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7.170 Coralline Algal Disease in Th
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7.179 Physiological Effects Of Aspe
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7.187 Characterizing Surface Microo
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7.195 How Quickly Does gorgonia Ven
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7.203 Spatial and temporal variabil
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8.210 Quorum Sensing Inhibitory Act
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8.218 Bacterial Communities Associa
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8.226 Bacterial Growth On Coral Muc
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8.234 Functional Diversity of Micro
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8.242 Microbial Community Profile O
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9.248 Chemistry And Ecology Of A Co
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Poster Mini-Symposium 11: From Mole
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12.413 Spatial Patterns Of Stony Co
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Poster Mini-Symposium 13: Evolution
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Poster Mini-Symposium 13: Evolution
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14.432 Gene flow of Symbiodinium on
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14.441 Population Genetics Of Spott
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14.449 Mitochondrial Phylogeography
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14.457 Undirect Evidences On The Co
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14.466 South East African, High-Lat
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14.474 Population Genetic Structure
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14.483 Influences Of Wind-Wave Expo
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14.491 Distributions And Diversity
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14.499 Do Mangroves And Seagrass Be
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14.507 Genetic variation of the hyd
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Poster Mini-Symposium 15: Progress
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Poster Mini-Symposium 15: Progress
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Poster Mini-Symposium 16: Ecosystem
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Poster Mini-Symposium 17: Emerging
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18.599 A Palaeoecological Perspecti
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18.607 Susceptibility Of Corals To
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18.616 Coral Reefs in Costa Rican C
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18.624 Environmental Endocrine Disr
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18.633 Northern Acehnese Coral Reef
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18.641 The Status Of Coral Reefs in
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18.649 The Effects of Increased Sea
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18.658 “Changing Times, Changing
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18.666 Assessing Land Based Inputs
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18.674 Monitoring Of Coral Recovery
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18.682 Seasonal Investigation On St
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18.690 Assessment Of The Coral Reef
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18.698 Distribution Of Seagrasses i
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18.706 Coral Reef Monitoring in the
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18.714 Pacific-Wide Status Of The R
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18.722 Quantitative Underwater Ecol
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18.730 Community Structure Of Reef
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18.738 Morphological Variation In T
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18.746 Decade-Long (1998-2007) Tren
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18.755 Coral Community Composition
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18.763 Changes in Coral Reef Ecosys
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18.771 Bathymetric Distribution Of
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Poster Mini-Symposium 19: Biogeoche
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Poster Mini-Symposium 20: Modeling
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21.807 The Recreational Value Of Co
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21.815 Dilemma in Coral Conservatio
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22.821 Estimating Populations Of Tw
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22.829 Commercial Topshell, trochus
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22.837 Trajectories Of Ecosystem Ch
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22.845 Ornamental Fish Trade in The
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22.854 Short-Term Recovery Of Explo
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22.863 Marine Protected Areas: Boon
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22.871 Rotary Time-Lapse Photograph
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22.879 Assessing And Mapping The Di
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22.887 Spatial Variations in Elemen
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23.1004 Coral Reef Conservation Cam
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23.1014 Second And Third Order Mana
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23.1023 Why do Divers Dive Where Th
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23.1031 The Colonial Tunicate tridi
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23.1039 Effectiveness Of A Small Mp
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23.893 Man Made Stress Reliever? An
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23.901 Reef Monitoring Project For
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23.909 Patterns Of Spatial Variabil
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23.917 Culture And Updated Traditio
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23.925 Scientific Monitoring And Cu
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23.934 Characterizing Local Stakeho
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23.942 Challenges in Coral Reef Man
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23.951 Coral Reef-Based Tourism And
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23.959 Marine Protected Area Report
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23.967 Reef Watch Monitoring And Ho
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23.975 A Comparison Of The Permanen
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23.984 Damselfish Embryo Assay: Fie
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23.992 The Decline Of Coral Reef Co
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24.1043 Characteristics Of Seagrass
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24.1051 Mass Culture Of acropora Co
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24.1059 Identifying Sediment-Tolera
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24.1067 Growth Of Newly Settled Ree
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24.1076 Herbivore Effects On Coral
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24.1084 Coral Reefs Conservation Pr
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24.1092 Lessons Learned On Demonstr
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24.1100 Proceedings in Shipgroundin
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24.1108 Restoring An Artificial "En
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24.1116 A Newly Established Coral R
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24.1124 Is The Scale Of Your Coral
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Poster Mini-Symposium 25: Predictin
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Poster Mini-Symposium 26: Biodivers
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Memo ..............................
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Authors INDEX Author Session Page A
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11th ICRS Abstract book - Nova Southeastern University

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