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profile and deposits a ridge. Each ridge represents a paleo-sea-level position. The best estimate of paleo-sea-level position can be assumed to be somewhere between the ridge crest and the toe of the shoreface. The boundaries between beach ridge sets may indicate a change in sea-level position. Where adjacent sets have a measurable elevation difference there has been a change in sea level (Tanner et al., 1989). Figure 1.7 illustrates Tanner’s theory of beach ridge formation. As an alternative to this theory, Curray (1996) re-proposed that offshore bars are built to sea level when sufficient sand is supplied to the coastline. If enough sand is available, the bar becomes emergent during periods of low surf. With the subsequent rise and fall of tides, and if surf conditions remain low, the bar will grow in height. Taylor and Stone (1996) proposed that during storm activity, sand from existing ridges is eroded and stored in an offshore bar. During calm weather conditions, the sand is transported onshore and a ridge is rebuilt. Each beach ridge plain displays the same relative time sequence. The ridge closest to the mainland is oldest and the ridge immediately adjacent to the beach is youngest. All others fit in a sequence between the two extremes (Tanner, 1988). Since ridges form on the beach face, they are indicators of the orientation of the coastline and approximate the vertical position of sea level at the time of their deposition (Donoghue and Tanner, 1992; Fernald and Purdum, 1992; Tanner, 1988). A beach ridge plain can be divided into sets. The different orientations of the sets indicate changes in oceanographic conditions (sea level rise, changes in river mouth position) or a change in the rate of sediment supply (Curray et al., 1969; Dominguez et al., 1992). Many of Florida’s barrier islands are composed of beach ridges. The organization and the physical character of the beach ridges that make up the Holocene beach ridge plains of the northwest Florida barrier islands can be employed to study the depositional history of the barriers. Sea-Level Change Sea level is never static, but rather has fluctuated throughout geologic time. Several factors can cause these fluctuations including changes in the volume of seawater (i.e. thermal expansion and contraction, or advance and retreat of ice sheets), rise and fall of the land or ocean floor (i.e. tectonics, isostatic rebound) and variations in the earth’s gravitational field (the gravitational forces between the sun and moon will change the distribution of the earth’s water 9
and, therefore, sea level) (Dorsey, 1997). The earliest reported systematic sea-level measurements were begun in 1682 at Amsterdam (van Veen, 1954), 1732 at Venice (Ekman, 1988) and 1774 at Stockholm (Pirazzoli, 1974; Zendrini, 1802). The construction of a sea-level curve is based on having paleoshoreline indicators (shell, peat etc) that are datable. Once samples have been dated, a curve showing the details of rise or fall of sea level in a given region can then be generated. Suess was the first to take up the idea of global sea-level change (Fairbridge, 1961). Since these early sea-level studies, many global and local sea-level curves have been created. Comprehensive treatments include that of Bloom (1977), who published an atlas of sea- level curves. Pirazzoli (1991) provides a global compilation of Holocene sea-level curves. Pre-Holocene Sea level Intensive study of late Quaternary sea-level change came about in the 1950s with the advent of radiocarbon dating techniques (Balsillie and Donoghue, 2004). By the 1960s it was clear that Quaternary sea-level history could be characterized by three modes of behavior (oscillating, smooth and continuously rising and smooth and continuously rising followed by stability at or near current mean sea level). Fairbridge (1961) presented an oscillating curve. This curve rose rapidly from the early Holocene to about 6,000 years B.P. It then oscillated about current mean sea level. Shepard (1963, 1964) produced a smooth curve that rose to present mean sea level. The third mode of behavior was suggested by Fisk (1956), Godwin et al. (1958) and McFarlan (1961). They proposed a smooth, continuously rising curve from the early Holocene to about 5,500 years ago, followed by sea level stability at or near current mean sea level. The oscillating mode is the currently accepted model and the model used in this investigation as depicted in Figure 1.5. Sea-level change during the Quaternary was primarily a result of the cyclic growth and decay of ice sheets (Lambeck and Chappell, 2001). Glacial periods were times of sea-level lowstands and interglacial periods were times of sea-level highstands (Lambeck and Chappell, 2001). A number of indicators have been used as evidence of past sea-level change. These include raised or submerged shorelines (i.e. beach ridges or shorelines indicated by fossil coral reefs above present growth positions or submerged in-situ tree stumps, erosional features like shore platforms and marine notches (Lambeck and Chappell, 2001). The onset of the most 10
Page 1 and 2: THE FLORIDA STATE UNIVERSITY COLLEG
Page 3 and 4: ACKNOWLEDGEMENTS I would like to th
Page 5 and 6: 4. RESULTS Laboratory Analyses ....
Page 7 and 8: LIST OF FIGURES 1.1 Location map of
Page 9 and 10: preheating is carried out on a heat
Page 11 and 12: 4.17 Site SVI 023. a) Trench. b) Sa
Page 13 and 14: 4.38 Location relative to the Apala
Page 15 and 16: A.37 Granplot analysis of sample 05
Page 17 and 18: A.83 Granplot analysis of sample 05
Page 19 and 20: ABSTRACT The goal of this investiga
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Page 23 and 24: the rate of erosion or deposition a
Page 25 and 26: esult of the buildup of offshore ba
Page 27: Recent studies of barriers using Gr
Page 31 and 32: Holocene Sea Level Over 900 Holocen
Page 33 and 34: first is that sea level rose steadi
Page 35 and 36: Figure 1.2. Beach ridge sets on St.
Page 37 and 38: -100 Figure 1.4. Pleistocene glacia
Page 39 and 40: Figure 1.6. The Apalachicola River
Page 41 and 42: Figure 1.8. Global sea-level histor
Page 43 and 44: K and L have crest elevations of ap
Page 45 and 46: Geoarchaeology The earliest inhabit
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Page 53 and 54: At each vibracore or trench locatio
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Page 57 and 58: Application of OSL to Coastal Studi
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Page 61 and 62: Topographic Surveying Topographic s
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Page 67 and 68: Increasing energy T CONDUCTION BAND
Page 69 and 70: Figure 3.5. Sample removed from lar
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Page 75 and 76: Sample Sites CHAPTER 4 RESULTS A to
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collapsed the trench. Therefore, a
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SVI025 This site is located within
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m and 3.7 m respectively. A cross s
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Vincent Island has changed little o
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(sorting). Standard deviation decre
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4,100 and 3,500 years ago. The corr
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Table 4.1 Continued Site Samples Be
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Table 4.3. Measured elevations of S
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Table 4.5. Application of Tanner’
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Table 4.7. OSL age calculations usi
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Table 4.9. Paleosealevel position e
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Figure 4.2. Example of a trench thr
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Figure 4.5. Site SVI 003. Trench ex
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a) b) 050505-01E 050505-01K 050505-
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a) b) 050505-04C 050505-04A Figure
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Figure 4.13. Site SVI 015. Vibracor
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a) b) 011006-15 011006-16 Figure 4.
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a) b) 011106-08 011106-07 011106-10
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Figure 4.21. Dutch gouge-auger core
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Figure 4.23. Line A-A’ represents
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Elevation (m) NAVD 88 5.00 4.50 4.0
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1200 +/- 100 yr 102 Figure 4.27. GP
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0.65 Set C 0.6 0.55 0.5 Set A 0.45
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6 Set B Set C Set E 5 Set A Set F S
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0.7 Set C 0.6 Set A 0.5 Set E Set F
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ENVIRONMENTS OF DEPOSITION -- SKEWN
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mean grain size (phi) 3 2.5 2 1.5 1
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SVI 015 SVI 002 SVI 003 114 SVI 004
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CHAPTER 5 DISCUSSION The beach ridg
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vibracore or trench, both of which
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Skewness can be used to identify th
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island. Another is a C-14 date of 2
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sea level. It was at this point tha
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The fourth hypothesis was that sea-
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APPENDIX A INDIVIDUAL SIEVE ANALYSI
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Berger, G., 1988, Dating quaternary
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Douglas, B., Kearney, M. and Leathe
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Jol, H.M., Peterson, C.D., Vanderbu
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Northwest Florida Water Management
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Stapor, F.W. and Tanner, W.F., 1977
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BIOGRAPHICAL SKETCH Beth Margaret F
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