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Knorr, Paul Octavius.
The case for high-order, pleistocene sea-level fluctuations in Southwest Florida
h [electronic resource] /
by Paul Octavius Knorr.
[Tampa, Fla] :
b University of South Florida,
ABSTRACT: Florida's Plio-Pleistocene strata record episodes of sea-level highstands. The age of the strata is often ambiguous as there are no consistently reliable dating techniques that can be unequivocally applied to many of the units. The lack of preservation of continuous Plio-Pleistocene sedimentary sequences is a consequence of Pleistocene mean sea-levels not flooding peninsular Florida, the low volume of sedimentary supply, and the lack of new accommodation space. This study investigates a 6 m cyclothem-type set of six shallow-marine shell beds separated by five subaerially exposed packstone beds. These strata are part of the biostratigraphically-defined early Pleistocene (1.1 --^ 1.6 Ma) Bermont formation and were likely deposited during a 160 kyr interval between 1.3 and 1.1 Ma. The shell beds are mollusk-rich and contain moderately well-sorted fine sands. The packstones contain sparry calcite cements and show evidence of subaerial weathering, such as an irregular upper solution surface, root molds, and sparry freshwater calcite cements. The upper surfaces of the packstones are unconformities that separate five episodes of highstand deposition. A grain-size analysis shows an upward-coarsening trend between depositional episodes, which most likely indicates a progressively decreasing water depth. The bivalve assemblages suggest a mean paleodepth during the deposition of the shell beds of approximately 7.5 m; alternatively, in situ Anodontia alba, which colonized these units after deposition, point to a depth of 1 m. A subsidence rate of 6 m/Ma is inferred from the thickness of deposits near the locality. Based on a comparison of the height of the strata with ex isting eustatic curves, the early Pleistocene age of the formation, and the 6 m/Ma subsidence rate, the most parsimonious duration for the interval between the cyclothems is 41 kyr, dominantly forced by obliquity orbital variability. Combining the data indicates that the early Pleistocene sea level was between 11.2 and 14.4 m above sea level (asl); previous estimates of early Pleistocene highstands have shown an elevation approximately 15 m asl. If the 1 m depth of Anodontia alba is used, the depth was likely 6.3 m asl.
Thesis (M.S.)--University of South Florida, 2006.
Includes bibliographical references.
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Adviser: Peter Harries, Ph.D.
t USF Electronic Theses and Dissertations.
The Case for High-Order, Pleistocene SeaLevel Fluctuations in Southwest Florida by Paul Octavius Knorr A thesis submitted in partial fulfillment of the requirements for the degree of Master of Science Department of Geology College of Arts and Sciences University of South Florida Major Professor: Pe ter Harries, Ph.D. Gregory Herbert, Ph.D. Eric Oches, Ph.D. Date of Approval: July 26, 2006 Keywords: cyclothem, Bermont, stratigraphy, subaerial exposure, mollusk, subsidence Copyright 2006, Paul Octavius Knorr
For Jenn and Andrew, the two shining stars of my life.
Acknowledgements I would like to thank my major professo r, Dr. Peter Harries, for his guidance, support, and understanding over the last two years. His profound breadth and depth of paleontological, paleoecological, and stratigraphical knowledge as well as his dedication to quality research are inspiring. Additionally, many thanks to Dr. Eric Oc hes and Dr. Gregory Herbert for sharing their insights and enthusiasm about all things geological. Thanks to Dr. Al Hine for sparking my interest in sequence stratigraphy in the first place. A very special thanks goes to the 2005 REU team: Jennifer, Rachel, Leila, Troy, Katie, Bill, Patricia, Paul, and Sarah. Without their efforts, far more of my own sweat and blood would have been shed over the final year of my research. Their contributions are much appreciated and have been sp ecifically referenced as appropriate. Finally, I would like to recognize the National Science Foundation for funding the main project, namely the aforementioned REU, of which my own research has been a small part.
i Table of Contents List of Tables iii List of Figures iv Abstract vi Chapter One Introduction 1 The Nature of Sea-Level Change in Florida 1 Brief Overview of the Longan Lakes Study Locality 2 Depositional Framework 7 Subsidence Rates 9 Chapter Two The Pleistocene Bermont Formation at Longan Lakes 11 The Bermont Formation 11 Difficulty of Determining Age of Strata 17 The Age of the Bermont Formation 19 Chapter Three Materials and Methods 22 Chapter Four Results 24 Evidence of Subaerial Exposure in Packstone Beds 24 Water Depth During Deposition of Shell Beds 32 Bivalve and Gastropod Analysis 34 Chapter Five Models of Sea-Level Change 37 Sequence Stratigraphy 37 Cyclostratigraphy 38 Orbital Forcing by Obliquity 40 Fischer Plots and the Relationship be tween Time and Cycle Thickness 41 Correlation of the LL Bermont Strata with a Eustatic Curve 43 Impacts of Uplift and Subsidence 49 Modelling Early Pleistocene Sea-Le vels with the Bermont Strata 51
ii Chapter Six Conclusions 54 References Cited 56 Appendices 70 Appendix A: Lithologic Data 71 Appendix B: Grain-size Data 78 Appendix C: Bivalve Data 82
iii List of Tables Table 1. Weighted Average Minimum Biva lve Depth for Longan Lakes Shell Beds. 36 Table 2. Duration of Sea-Level Cycle Orders. 39 Table 3. Summary of Interval Characterist ics within the Longan Lakes Sequence. 42 Table 4. Summary of Early Pleist ocene Interval Characteristics. 47 Table 5. Summary of Grain Size Analysis. 78 Table 6. Sorting Coefficient by Bed. 79 Table 7. Weighted Average Bivalve Depth in Meters for Representative Beds from LL. 82 Table 8. Weighted Average Bivalve Depth per Cycle. 83
iv List of Figures Figure 1. Overview of Florida geology. 3 Figure 2. Simplified stratigraphy of the Berm ont formation at Longan Lakes. 4 Figure 3. Recent sea-level. 5 Figure 4. + 13 m early Pleistocen e high sea level (1.2 Ma). 6 Figure 5. Stratigraphic column of early Pl eistocene Bermont formation at LL Quarry. 13 Figure 6. Longan Lakes Quarry strata. 14 Figure 7. Close-up of packstone bed 3a (above scale) overly ing shell bed 3b. 14 Figure 8. Small-scale karstic collapse. 25 Figure 9. Bed 2a, Alizarin Red S staining (X20). 27 Figure 10. Bed 2a, Alizarin Red S staining (X30). 28 Figure 11. Bed 3a, Alizarin Red S staining (X100). 28 Figure 12. Bed 3a, etched surface (X30). 29 Figure 13. Bed 4a, Titan Yellow staining (X20). 29 Figure 14. Bed 5a, Alizarin Red S staining (X10). 30 Figure 15. Bed 6a, Titan Yellow staining (X30). 30 Figure 16. Bed 6a, etched (X70). 31 Figure 17. Cumulative grain sizes fo r lower portions of shell beds. 33 Figure 18. Fischer plot fo r Longan Lakes strata. 42 Figure 19. Bermont-age eustatic fluctuati ons correlated with Longan Lakes strata. 46
v Figure 20. Spatial relations of the Be rmont formation at Longan Lakes. 52 Figure 21. + 6.3 m Pleistocene high sea level based on Anodontia alba (1.2 Ma). 53 Figure 22. Cumulativ e grain sizes. 80 Figure 23. Cumulativ e grain sizes. 81
vi The Case for High-Order, Pleistocene Sea-Level Fluctuations in Southwest Florida Paul Octavius Knorr ABSTRACT Floridas Plio-Pleistocene strata record episodes of sea-level highstands. The age of the strata is often ambiguous as there are no consistently reliable dating techniques that can be unequivocally applied to many of the units. The lack of preservation of continuous Plio-Pleistocene se dimentary sequences is a cons equence of Pleistocene mean sea-levels not flooding peninsular Florida, the low volume of sedimentary supply, and the lack of new accommodation space. This study in vestigates a 6 m cyclothem-type set of six shallow-marine shell beds separated by five subaerially exposed packstone beds. These strata are part of the biostratigraphi cally-defined early Pl eistocene (1.1 1.6 Ma) Bermont formation and were likely deposited during a 160 kyr interval between 1.3 and 1.1 Ma. The shell beds are mollusk-rich and contai n moderately well-sorted fine sands. The packstones contain sparry calcite cements and show evidence of subaerial weathering, such as an irregular upper solution surface, root molds, and sparry freshwater calcite cements. The upper surfaces of the packstones are unconformities that separate five episodes of highstand deposition. A grain-size analysis shows an upwardcoarsening trend between depositional episodes, which most likely indicates a progressively decreasi ng water depth. The
vii bivalve assemblages suggest a mean paleodepth during the deposition of the shell beds of approximately 7.5 m; alternatively, in situ Anodontia alba, which colonized these units after deposition, point to a dept h of 1 m. A subsidence rate of 6 m/Ma is inferred from the thickness of deposits near the locality. Based on a comparison of the height of the strata with existing eustatic curves, the early Pleistocene age of the formation, and the 6 m/Ma subsidence rate, the most parsimonious duration for the interval betw een the cyclothems is 41 kyr, dominantly forced by obliquity orbital variability. Combining the data indicates that the early Pleistocene sea level was be tween 11.2 and 14.4 m above sea level (asl); previous estimates of early Pleistocene highstands ha ve shown an elevation approximately 15 m asl. If the 1 m depth of Anodontia alba is used, the depth was likely 6.3 m asl.
1 Chapter One Introduction The Nature of Sea-Level Change in Florida The links between changes in the Eart hs orbital parameters, glaciation, and absolute sea level are well established (e.g., Hays et al., 1976; Zachos et al., 2001). The Florida Platform has a low-gradient slope (Hine et al., 2003) and low surface relief (Schmidt, 1997), so small fluctuations in sea le vel can expose or submerge large areas of the shelf in a geologically short amount of tim e. Marine deposits are preserved primarily during periods of peak transgression (Emery and Myers, 1996), therefore Floridas PlioPleistocene geologic column at any specific location is, as Charles Lyell proclaimed of the entire geologic record, an imperfect recor d. Florida stratigraphy records a series of discrete intervals rather than a temporally complete continuum. Because current sea level is relatively high compared to much of the past 3 Ma (e.g., Hallam, 1992), for most of this interval sea level was necessari ly below the current level; therefore, only a minority of earlier marine deposits have th e potential of being preserved in locations that are today emer gent. As a consequence of the Florida platforms tectonic stability (Smith and Lo rd, 1997), strata that were deposited during times of lower sea level relative to the Recent are located offshore or have been reworked, notwithstanding localized pockets of accommodation space (Scott, 1997), such as valley-fill sequences, or putative uplift due to karstification (Opdyke et al., 1984).
2 As a result of these limitations, Florid as strata can be used as a sea-level dipstick in which highstands are recorded in a series of episodic snapshots. Unfortunately, as will be demonstrated later in the study, it is hard to assign a numerical age to many of these deposits and, therefore, the temporal position of these deposits is difficult to constrain precisely. Floridas stratigraphy, shown in Figur e 1, dominantly reflects the highstand intervals of sea-level fluctuations. During the Miocene, thick, phosphate-rich strata collectively assigned to the Hawthorn Group we re deposited during multiple intervals of high sea level (Scott, 1997). After a pronounced Late Miocene sea level fall, Pliocene sea levels rose and deposited a patchy ven eer of fossiliferous strata, including the Tamiami and the Caloosahatchee formations, across the peninsula (Scott, 1997). At the same time the Isthmus of Panama closed completely, changing ocean current and salinity patterns in the Gulf of Mexico and affecting the extent of no rthern sea ice (Coates et al., 1992, 2004; Driscoll and Haug, 1998; Ruddiman, 2001). Brief Overview of the Longan Lakes Study Locality This study will focus on a cyclothem-type (sensu Wilson, 1975) set of shallowmarine shell beds and subaerially-exposed packstone beds that are part of the informally named Pleistocene Bermont formation (Lyons, 1991). The strata, located at the Longan Lakes Quarry (LL) near Immokalee, Flor ida, are shown in Figure 2. A detailed description will be provided later in this study. Relative to strata being deposited in areas of high tectonic subsidence (e.g. New Zealand) the LL strata are co mparatively thin; the height of the column totals less than 6 m and represents an interval that might be as long
as 600 kyr, based on a synthesis study by Lyons (1991). In all, six shell beds separated by five subaerially-exposed packstone beds were documented at the LL locality. By comparison, New Zealands Wanganui basin hosts a 1-km-thick, continuous PlioPleistocene sequence composed of 20 individual prograd ational cycles that were deposited in 1 Ma (Naish and Kamp, 1997). Figure 1. Overview of Florida geology. Figure synthesized from Stanley (1986), Lyons (1991), Allmon et al. (1996), Haug et al. (1998), and Herbert (2004). 3
The Bermont formation, shown in Figure 2, was probably deposited in the early Pleistocene between 1.6 Ma and 1.1 Ma (Lyons, 1991) during a period of relative glacial quiescence that lasted from 1.5 Ma thr ough 1.0 Ma (Richmond and Fullerton, 1986). The frequency of sea-level fluctuations cha nged between 1.2 Ma and 0.65 Ma, transitioning from low-amplitude 41 kyr cycles to hi gh-amplitude 100 kyr cycles (Diekmann and Kuhn, 2002). The subsequent late Pleistocene high-amplitude, sea-level fluctuations are characterized by a slow accumulation of ice followed by rapid deglaciations resulting in asymmetric sea-level fluctuations; the late Pleistocene Fort Thompson formation is a product of this paleoclimatic control. 4 Figure 2. Simplified stratigraphy of the Bermont formation at Longan Lakes.
To help visualize the extent of Pleist ocene sea-level highstands, two sea-level reconstructions are presented: 1) a representa tion of modern sea level (Fig. 3); and 2) a reconstruction of a +13 m sea le vel stand that is inferred fo r the LL Bermont strata, which are the subject of this study (Fig. 4). Because modern elevations were used to create the maps, Figure 4 is representative only of the ar ea that was submerged; the specific coastal morphology is likely to have been different. Figure 3. Recent sea-level. 5
Figure 4. + 13 m early Pleist ocene high sea level (1.2 Ma). 6
7 Depositional Framework Peninsular Florida, located on the Florid a Platform, hosts some of the worlds most expansive and taxonomically diverse sh ell beds. The Fort Thompson, Bermont, and Caloosahatchee formations, shown in Figure 1, occupy three important Plio-Pleistocene portions of Floridas stratigraphic column (Sco tt, 1992). However, because of the limited volume of accommodation space, the Fort Thompson, Bermont, and Caloosahatchee formations are not generally exposed within a single stratigraphic se ction. The volume of accommodation space is restricted by the low subsidence rate of the Florida Platform (Mullins and Neumann, 1979) as well as th e low-gradient slope (1:2,000 to 1:5,000) of the underlying carbonate ramp (Hine et al., 200 3). A high rate of subsidence coupled with high sediment supply is conducive to preservation, as evidenced by Naish and Kamps (1997) study of New Zealands Wanganu i basin; the low subsidence rate of the Florida platform (Mullins and Neumann, 1979), c oupled with low siliciclastic input, is conversely a major reason for the lack of preservation of continuous Pliocene and Pleistocene sedimentary sequences. Another reason that portions of Florida s Plio-Pleistocene column are dominated by non-deposition is due to the elevation of peninsular Florida relative to paleo-sea levels. The currently emergent portions of the Florida platform were generally not submerged during the Plio-Pleistocenes non-highstand intervals. It should be noted that pockets of accommodation space have been created intermittently by fluvial erosion and karsti fication during sea-level lowstands (Allmon, 1992; Scott, 1997; Ferguson and Davis, 2003). Also, thicker sedimentary sequences
8 appear along the platforms southern marg in where carbonate environments dominate (Perkins, 1977). As a result of the limited accommodation space, Pleistocene deposits of southern Florida are characterized by thin and disc ontinuous deposits (DuBar, 1974; Missimer, 1992; Zullo and Harris, 1992) that represen t the stranded remnants of highstand sequences (Harris and Zullo, 1993; Hine et al., 2001). An additional consequence of the limited accommodation space is that portions of older deposits were eroded and reworked during sea-level lowstands. Some of these sediments were then incorporated into later deposits (Davis, 1994b; Hine et al., 2003). Eroded and rewo rked Miocene and Pliocene sediments provide the siliciclastic material for Pleistocene deposits (Scott, 1997). Deposition is also impacted by the degr ee of relief along th e pre-depositional surface. High-relief (relative to surr ounding geomorphology) pale okarst topography and the incision of paleodrainages can provide in creased accommodation space in the form of voids and provide areas that favor sedimentary accumulation (Allmon, 1992). As a result, the thickness of a formation may vary by orders of magnitude over small distances, as thicker deposits accumulate in valleys and thinner deposits cap the surrounding highlands (Scott, 1997; Duncan et al., 2003; Ferguson and Davis, 2003); the contribution of any given formation to a particular outcrop is often ambiguous and uncertain, over distances that range from over 100 km (Lyons, 1992) to tens of meters (Allmon, 1992). To further complicate matters, there is a l ack of consensus over the ages of the Fort Thompson, Bermont, and Caloosahatchee formations, caused in large part by the lack of suitable numerical dating methods fo r the early Pleistocene (Lyons, 1991; Scott,
9 1992). This combination of laterally di scontinuous deposition and chronologic uncertainty hampers the interpretation of Pl eistocene sea-level behavior in Florida. On a local scale, it can be difficult to pinpoint the processes that lead to the formation of shell beds (Allmon, 1992). For ex ample, changes in sedimentation rates and dissolution processes can both impact a de positional cycles lithological end-product (Kidwell, 1986; Allmon, 1992). A study by Roof et al. (1991) of Plio-Pleistocene sediments recovered from the northwester n portion of the West Florida carbonate platform indicated that pattern of regi onal sedimentary depositional cycles passed through three stages: from 5.4 to 2.8 Ma the se dimentation was aperiodic, from 2.8 Ma to 0.8 Ma it was dominated by 30to 60-kyr cy cles that were a c onsequence of 41 kyr orbital periodicity, and from 0.8 Ma to the present sedimentation has been dominated by 100-kyr cyclicity. That study also found it like ly that the provenan ce of the sediments was the Mississippi River delta, and that th e greater portion of sand-sized and larger material was diverted or depos ited before the Loop Current could carry it to the West Florida carbonate platform (Roof et al., 1991). A Miocene influx of sediment to peninsular Florida from the Appalachian M ountains (Scott, 1997) is postulated as an additional source of siliciclastic material. Subsidence Rates Specific rates of subsidence are difficult to quantify in absolute terms, especially on passive margins. However, the relative ra te of subsidence or uplift compared to eustatic change is more impor tant to sedimentary deposition or erosion than the absolute rate. Mullins and Neuman (1979) used drill-hole da ta to calculate a rate of 18 m/Ma for
10 the Oligocene-Holocene in the South Florida-Bahamas region. The area for which the rate was calculated includes the Miami Terrace, a part of the East Florida Slope (Hine, 1997) and, therefore, a part of the Florida Pl atform. A similar rate, 19 m/Myr, based on well data ranging to the mid-Miocene is gi ven for the central west Florida carbonate platform (Mullins et al., 1988). However, existing cross-sections of the south Florida platform demonstrate that subsidence, if present, is most likely differe ntial, with greater va lues (i.e., 18 m/Myr) to the east and lesser valu es (calculated below) to th e west (Warzeski et al., 1996; Cunningham et al., 2001). To quantify subsidence, the height of two cross-sections showing the thickness of the Miocene Peace Ri ver Formation were measured. The two points used, W-16523 (Warzeski et al., 1996) and W-17534 (Cunningham et al., 2001), are well points (rather than interpolated portions) and are 29 km and 31 km, respectively, from the LL locality. In order to apply the mo st conservative approach, which yields the lowest subsidence rates, the ea rliest and latest dates (Compton, 1997) for the Peace River Formation, from the early Middle Miocene ( 16.4 Ma) to Early Pliocene (3.6 Ma), are used as the duration of the formation. The two measured sections were approximately 60 m (Warzeski et al., 1996) and 90 m (Cunningham et al., 2001) thick. Thus, the two subsidence rates are 5 m/Myr, and 7 m/Myr, respectively. The mean of these two values, 6 m/Myr, w ill be used as the subsidence rate for the LL site. This subsidence rate provides re asonable values when compared to existing cross-sections and estimates of sediment thickness in south Florida (Warzeski et al., 1996; Scott, 1997; Cunningham et al., 1998; 2001; 2005).
11 Chapter Two The Pleistocene Bermont Formation at Longan Lakes The Bermont Formation Lyons (1991) published a comprehensive summary of the various chronostratigraphic approaches that have been applied to Florid as Plio-Pleistocene faunal assemblages. The beds that contai n these faunal assemblages, incorrectly and informally defined as formations using biostratigraphy, represent a significant portion of the near-surface strata of the sout h Florida peninsula (Scott, 1997). In accordance with accepted stratigraphic guidelines (NACSN, 2005), Scott (1992) placed these assorted faunal assembla ges and their associat ed strata into the informally named Okeechobee formation, defined solely on the basis of lithostratigraphy. The Okeechobee formation incorporates the Fort Thompson, Bermont, and Caloosahatchee formations as faunas. Howe ver, to conform with current usage among the majority of researchers of Floridas Ne ogene, the units will be referred to as formations, albeit informally named and defi ned on the basis of biostratigraphy. A more appropriate classification w ould be assemblage biozone or allostratigraphic units (NACSN, 2005), but formal biostratigraphic de finition of these three formations is beyond the scope of this study. The active LL quarry is located approximate ly 30 km east of the Gulf of Mexico at 26.21.22N, 81.33.53W, North American Datum 1927 (see Fig. 2). The elevation at the
12 surface of the quarry is 6.4 m above mean sea level (msl). The stratig raphic section that is described in this study is located at an elevation between 4.4 m below msl and 0.6 m above msl. The strata exposed at LL consist of si x lithologically and depositionally similar meter-scale unconsolidated shell beds; five of the shell beds are capped by packstone beds formed by diagenetic alte ration during subaerial exposure prior to burial by the next shell bed. A stratigraphic column depicting th is relationship is pr ovided in Figure 5. A photograph of the entire section is provi ded as Figure 6, and a close-up photograph showing a contact between a shell bed and a packstone bed is pr ovided as Figure 7. Additionally, a description of each bed is provided in Appendix A. As will be demonstrated later, the LL beds contain fossil material from the early Pleistocene Bermont fauna. The shell beds consist of meter-scale se quences of unconsolidated bivalve and gastropod fragments within a moderately we ll-sorted fine sand matrix. Based on the molluscan taxa found in the shell beds, the be ds appear to have been deposited in a nearshore marine environment. The packstones (Dunham, 1962; Embry a nd Klovan, 1972) contain both sparry calcite cements and secondary micrite. The packstones show evidence of subaerial weathering, specifically an irregular upper solu tion surface, root molds, solution cavities, and sparite cements. There are no signs of soil development beyond the root molds and that material was likely stripped off duri ng the subsequent tran sgression. The upper surfaces of these packstones form the unc onformities that bound distinct episodes of
Figure 5. Stratigraphic column of early Pleistocene Bermont formation at LL Quarry. 13
Figure 6. Longan Lakes Quarry strata. The Be rmont formation encompasses the lower half of the photo and is approximately five meters high. Figure 7. Close-up of packstone bed 3a (above scale) overlying shell bed 3b. Scale is approximately 20 cm long. 14
15 highstand deposition. A model for the proposed sequence of events leading to the formation of these packstone beds is: 1. An unconsolidated, nearshore shell be d is deposited, as evidenced by the grains and shells found in the packstone. 2. After eustatic fall of sea level, the sh ell beds were subaerially exposed, or at least located in the meteoric vados e zone in close proximity to the land surface. An influx of water undersaturated in calcium, derived from convective rainfall (Chen and Gerber 1990) falling on the newly exposed carbonate surface, leads to the deve lopment of characteristic karst features, most notably cementati on followed by increased secondary porosity (Wright, 1982). 3. The increased amounts of the rainfall th at led to karstification also cause meteoric (freshwater) water to accumula te at the top of the phreatic zone. Shell beds are ultimately cemented in the vadose zone with freshwater sparite (Wright, 1982). 4. Sea level begins to rise, scouring the upper surface of the now-cemented bed and then depositing an overlying shell bed, thus renewing the cycle. Shell beds and packstone be ds are similar from one layer to the next and cannot be distinguished from one another visually. However, minor variations of the faunal content between the six shell bed layers have been documented. Specifically, changes in molluscan species richness and evenness, guild structure, and comm unity structure have been noted between the cycles (Banasiak et al., 2006; Chelladu rai et al., 2006; Greene et al., 2006). Despite these variations, the beds as a whole consistently contain key faunal
16 components of the Bermont formation. The te mporal relationship between the strata is unclear, but they appear to doc ument an uninterrupted series of cycles of transgression and regression. This will be disc ussed in greater detail below. The Bermont formation is lithologically and faunally similar to both the Caloosahatchee and the Fort Thompson formations. The Bermont formation is characterized primarily by tw o criteria: 1) the absence of a number of typical Caloosahatchee species; and 2) the presence of a few species that are found in the Fort Thompson and absent from the Caloosahatchee (DuBar, 1962; 1974). The following biostratigraphically dia gnostic bivalve and gastropod taxa, all present in the LL shell beds, have been documented from the Bermont and younger units (DuBar, 1962; DuBar, 1974): Codakia orbicularis, Terebra concava Vokesinotus griffini, Anadara lienosa Chione elevata Arcinella cornuta Macrocallista maculata Alabina adamsi Oliva sayana, Strombus alatus, and Vermicularia spirata. Trachycardium muricatum and Nassarius albus have been documented from the Bermont and older units (DuBar, 1962; DuBar, 1974); bo th of these taxa are present in the LL shell beds Fasciolaria okeechobensis Nassarius albus, Sinistrofulgur roseae Strombus erici Strombus evergladesensis and Strombus lindae, all present in the LL shell beds, are documented as being exclusive to the Bermont (DuBar, 1962; 1974). Therefore, based on the presence of the aforementioned taxa, the LL beds correlate to the biostratigraphically defined Bermont formation.
17 Difficulty of Determining Age of Strata Dating of the LL beds is problematic. Amino acid racemization (AAR) can be used to obtain the relative age of fossils with ages ranging from several thousand to several million years (Oches and McCoy, 1995; Bradley, 1999); however, the technique is best suited for relative dating and for greatest accuracy requires calibration by an external, numerical dating method (Rutter et al., 1985; Miller and Br igham-Grette, 1989). The application of AAR holds promise in es tablishing the presence and continuity of cyclothem-type beds; if AAR demonstrates that the relative amount of time that separates the beds is constant, the presence and possi bly duration of cyclicity can be established (Sanford et al., 2006). Radioisotopic dating methods are expensiv e and not easily applied to marine deposits. Although the mineral glauconite, of marine origin, can be dated using 40 Ar/ 39 Ar dating (Bradley, 1999), the poten tial incorporation of Mio cene and Pliocene palimpsest sediments into Pleistocene strata (Scott, 1997) would produce unreliable results. Numerical dating by 234 U/ 238 U may be possible using diagene tically pristine fossil corals (McCartan et al., 1982; Schwarcz and Blackwe ll, 1985) although the result of recent work has been discouraging; for example, in a study by Muhs et al., all 14 of the Pleistocene coral samples analyzed failed to meet the closed-system conditions necessary for accurate dating (Muhs et al., 1992). In any event, 234 U/ 238 U dating has not been successful with samples that are older than approximately 400 ka, precluding its use to strata older than the Fort Thompson. Several cobble-size pieces of coral were embedded in the LL strata; however, they did not appear to have grown in situ and are thus of questi onable age relative to the
18 time of LL deposition. The coral appeared to have been broken off from larger pieces and showed signs of damage by transport. It is, therefore, uncertain whether the corals grew during the same sea level stand that led to the deposition of the beds in which they are found, or whether they are re mnants of reworked pre-existing strata, especially as the underlying Caloosahatchee in the region is dominated by reefal facies. As a result of the aforementioned difficulties, biostratigraphic zonation has been the primary method used to correlate Floridas Plio-Pleistocene strata Floridas diverse vertebrate faunal assemblages (MacFadden, 1997) were used, in combination with a suspect magnetostratigraphic approach and Sr 87 /Sr 86 chronology, to bracket the Bermont formation (Hulbert and Morgan, 1989; Webb et al., 1989); unfortunately, no identifiable vertebrate fragments were found at the LL locality. In any event, vertebrate biochronology does not have the resolution necessary to disti nguish the time that elapsed between the shell beds. Because they are far more common than vertebrates, assemblages of invertebrate fossils are typically used to differentiate and identify Plio-Pleistocene strata. The inclusion or omission of a series of fossils, typically mollusks, is the primary method of determining the relative age of a unit. The primary drawback to this method is the lack of age-resolution; the 21 kyr to 100 kyr range (e.g., Coe, 2003) of orbital periodicity cannot be resolved with invertebrate biostratigraphy. Despite these problems in constraining th e chronostratigraphic framework of the Florida Pleistocene, it is possible to investigat e aspects of the discontinuous nature of sealevel change in Florida during the Pleistocene. This will be accomplished by holistic integration of lithologic obs ervations, paleoecological information, and stratigraphic
19 principles. Although a robust sequence stratigr aphic model cannot be developed from the strata used in this study, li ght can be shed on the nature of higher-order sea-level fluctuations in the Pleistocene. The Age of the Bermont Formation Lyons (1991), in a comprehensive review and summary of the geochronology of Floridas Plio-Pleistocene formations, consid ers the probable ages of the Fort Thompson formation to be between 0.22 Ma and 0.95 Ma the Bermont formation between 1.1 Ma and 1.6 Ma, and the Caloosahatchee formati on between 1.8 Ma and 2.5 Ma (Fig. 1). These age ranges were established using a co mbination of radiometric dating methods as well as correlation with contemporaneous units in the Coastal Plain whose dates are welldocumented. Lyons (1991) arrived at the age range for the Bermont formation by synthesizing several existing studies, a brief summary of which follows. The Bermont has been alternately referred to as the Glades fo rmation by Vokes (1963), Unit A by Olsson (1964), Unit F by DuBar (1962), and more recently as a portion of the Bellegladean and the Loxahatchee faunas by Petuch (1993; 2003). DuBar later renamed Unit F the Bermont formation (1974), differentia ting the strata from the subjacent Caloosahatchee formation primarily by the ab sence of a number of biostratigraphically determinant taxa and the presence of a seve ral species not found in the Caloosahatchee. Critical gastropods named by DuBar (1974) that are restricted to the Bermont include: Fasciolaria okeechobensis Fusinus watermani Melongena bispinosa and Strombus
20 mayacensis; unfortunately, these key taxa are absent from the stratotype. A number of additional species have been added to the original list by later workers (Lyons, 1991). Early works placed the Bermont within the early Pleistocene (Vokes, 1963; Hoerle, 1970). Taylor (1966), as cited in Lyons (1991), considered it to belong to the late Pliocene or early Pleistocene. Based on Th 230 /U 234 and U 234 /U 238 ratios, Waller (1969), using Broeckers ((1969) as cited in Waller) data, considered the deposits to be early Pleistocene. DuBar (1974), however, consid ered the Bermont formation to be in the medial Pleistocene. Mitterer (1974; 1975) performed amino acid racemization analysis on a series of Floridian shells including Be rmont correlative material in the mid-1970s and, by applying a linear kinetics model, ge nerated an age of 324 ka for the underlying Caloosahatchee formation. Wehmiller and Belknap (1978), who found the linear nature of the model inappropriate, re -evaluated the data using a non-linear model and arrived at an age of 800 200 ka for the Bermont formation. To further complicate matters, the shells that were sampled were of uncertain or igin and may have been incorrectly assigned to the various units (Lyons, 1991). In the late 1980s, workers found beds cont aining terrestrial vert ebrate fossils in Hillsborough County that bracket the Bermont formation (Hulbert and Morgan, 1989; Webb et al., 1989). The overlying mammalian fa una are 1.5 Ma to 1.0 Ma in age and the underlying mammalian fauna is less than 1.7 Ma Webb et al. (1989) used a combination of magnetostratigraphy, stront ium isotope chronology of Chione elevata and mammalian biochronology to arrive at an overall age of 1.1 Ma to 1.66 Ma. Lyons (1991) found that the last set of values, 1.1 Ma to 1.6 Ma, corr elated well with Blackwelders M-3 interval-
21 zone (1981), an early Pleistocene Atlantic Coastal Plain mollusk zone which does not contain a Floridian equivalent. Thus, this study will follow the conclusi ons of Lyons (1991) and will use an age of 1.1 Ma to 1.6 Ma for the Bermont formation. In any event, although a few of the points made in this study rely on this speci fic time range, the majority of the points are still applicable if the beds are of a mo re recent (e.g., middle Pleistocene) origin. Given this age for the Bermont, then the formation and its fauna occupy a critical period of paleoecological and evolutionary transition between two paleoclimatically different epochs (Stanley, 1986; Imbrie et al., 1993). This was an interval during which communities and organisms responded to envi ronmental changes that were ultimately driven, at least in part, by the change of glaciation from a 41 kyr periodicity to 100 kyr periodicity (Imbrie et al., 1993). Because the early Pleistocene Longan Lakes Bermont formation deposits preserves a series of cy clical marine shell beds and subaerially exposed packstones, the post-extinction evolut ion of lineages and the response of faunal communities can be studied through a series of five chronologically distinct episodes.
22 Chapter Three Materials and Methods Three stratigraphically continuous bulk samples, approximately 20 l each, were collected from each bed as part of an NSFfunded, REU project. Thicker beds, or beds displaying variations in sedimentary struct ure and lithology, were subsampled. Each set of strata was surveyed relative to the local land surface using a Brunton compass and stadia rod. The elevation re lative to modern sea level wa s calculated by comparing the surveyed strata height to local land surface el evation as determined from USGS maps and digital elevation models. Upon returning to the laboratory, unlithifie d bulk samples were wet sieved and all material, including shell fragme nts and sediment, was retained. The fossil material from these samples was then sorted, identifie d, the presence and abundance of gastropod and bivalve species were tabulated, and a grain-size analysis of the sediment was performed. For each of the lithified units, thin sections we re prepared to investigate their diagenetic histories. In order to maintain continu ity, the specific details of each method are described in conjunction with the results and interpretation. The stratigraphy of the strata, the lithology of the beds, and thin sections of the packstone layers were used to identify the presence of the subaeria lly exposed layers. These subaerially exposed layers delineate five units that represent separate intervals of highstand deposition. The identification of gast ropods and bivalves were used to verify
23 that the LL strata are part of the Bermont fo rmation; furthermore, bivalve depth ranges were used to constrain the probable water de pth during the deposition of the shell beds. The grain-size analysis was used to determ ine if the mean water depth was constant during the deposition of each set of shell beds.
24 Chapter Four Results Several indicators of elevated and lowered sea levels were investigated to confirm and quantify the extent of sea level fluctuations at the LL locality. Indicators of subaerial exposure, and consequently lowered sea le vel, include the presence of freshwater cements, traces of dissolution on the upper surfaces of beds, root molds, and karstification. Characteristics of the strata at the outcrop and th in sections of the packstone beds were used to confirm that subaerial exposure occurred. Indicators of elevated sea level include the presence of abundant marine fossils in the shell beds. The depth range of occurrence of bivalve species pres ent in the shell beds was analyzed to determine the probable paleodepth during time of deposition. Additionally, a grain-size analysis was perf ormed to examine the relationship between depositional intervals. Evidence of Subaerial Exposure in Packstone Beds Strata that show signs of persistent s ubaerial exposure, for example the presence of freshwater cements, upper solution surf aces, root molds, and karstification, are indicators of intervals of lowe r sea level. Several indicator s suggest that the majority of the shells that constitute the sh ell beds at Longan Lakes were formed in the same cycle in which they are found. The composition of the bivalve assemblages between beds is
relatively consistent (Che lladurai et al., 2006) and in situ bivalves are present. When bivalves are found in life position, they are typically clustered in groups, so it is improbable that their position is the result of chance deposition after transport. Additionally, much of th e unfragmented shell material, even very thin shelled specimens, is in good condition and much of the ornament is virtually pristine, indicating that it has not been reworked by taphonomic processes (Dodd and Stanton, 1981). Dissolution cavities and root molds are pres ent in each of the subaerially exposed packstone beds, occupying 5-10 % of the volume of the packstone. Decimeter-scale changes in relief, apparently dissolution f eatures, were present on the upper surfaces of the packstone beds. Traces of root molds and secondary porosity, wh ich are indicators of subaerial exposure (Budd et al., 2002), were present in all the p ackstone beds. Postlithification molluscan boreholes are present on the upper surfaces of the packstone beds; these boreholes suggest that marine orga nisms inhabited these hardgrounds after cementation of the packstone but prior to the deposition of the overlyi ng shell-rich units. Figure 8. Small-scale karstic collapse. Collapse feature penetrates packstone bed 2a and connects shell beds 1c and 2b. 25
26 Karstic collapse was observed neither in the LL section that was studied in detail nor in the surrounding quarry walls, except in bed 2a. A collapse feature penetrating bed 2a approximately 10 cm wide and 10 cm high was noted and is shown in Figure 8; this conduit connected beds 1c and 2b. The f eature appears to have been caused by dissolution of bed 2a packstone, followed by a localized collapse, and subsequently by the intrusion of material from bed 1c. Ther e were no fragments of bed 2b found in either the underlying or overlying strata, so a mechani cal origin (e.g., collapse of bed 2a due to the weight of overburden) appears unlikely. Thus, the packstone beds appear to be an early merokarst rather th an a mature holokarst (sensu Dreybrodt, 1988). Thin sections were prepared for each of the packstone beds: LL-2a, LL-3a, LL-4a, LL-5a, and LL-6a. Five sets of thin secti on samples were then subjected to various treatments to elucidate the nature of the sediments and cements. The first set was a control, and was left unaltere d. The second set was etched wi th dilute HCl and washed in deionized water using the method outlined by Fr iedman (1959). The third set was etched with HCl and stained with Alizarin Red S di ssolved in dilute HC l (Friedman, 1959). The fourth set was etched in dilute acetic acid and stained with Clayton Yellow dissolved in NaOH and EDTA using the method outlined by Sc holle (1978) with some modifications as described by Choquette and Trusell (1978). The fifth set was impregnated with bluedyed casting resin by immersing the rock chip s in a blue resin bath inside a vacuum chamber for approximately fifteen minutes (A dams and MacKenzie, 1998). Thin sections were digitally imaged in plane polarized light using a Nikon SMZ-1500. A description of the char acteristics common to the five packstone beds is followed by characteristics specific to each be d; the implications of the findings are
summarized following the descriptions. A photograph representative of the beds is shown in Figure 9. All thin sections show indi cations of subaerial exposure in the form of secondary porosity (karst) and root molds. Over 50% of the grains are m oderately-sorted, wellrounded quartz. Abundant molluscan bioclast fragments, carbonate grains, and a small number of other grains including ph osphorite and dolomite are present. Micrite composed of low-Mg calcite fills over 50% of the space between grains. However, dissolution cavities, void space within biotic fragments, and root molds are almost uniformly filled with low-Mg calcite sparite. Sparry calcite, shown in Figures 10 and 11, is almost uniformly blocky cement or a drusy, mosaic, pore-filling cement. Trace amounts of circumgranular sparry calcite cemen t is visible on the e dges of grains that protrude into pore space. So me calcite crystals, usually with a dogtooth habit, are found precipitated on the insides of mollusk fragments. 27 Figure 9. Bed 2a, Alizarin Red S staining (X20). Photograph is representative of packstone beds and shows typical grain distribution and micritic matrix Stained portions (red) indicate calcite. Sparry calcite is often much lighter red than micrite due to differential absorption of stain and grain size.
Figure 10. Bed 2a, Alizarin Red S staining (X30 ). Meteoric sparry calcite precipitated within a dissolution cavity. Figure 11. Bed 3a, Alizarin Red S staining (X100). Closeup of meteoric calcite sparite in a root mold (cross-section). Observations specific to individual beds include: Bed 2a: Abundant pore space is present; some smaller pores are not completely filled with sparry calcite. 28
Bed 3a: Most root molds are almost completely filled with drusy mosaic sparry calcite (Fig. 13). Some dol omitization noted, typically coinciding with portions that appeared weathered. Figure 12. Bed 3a, etched surface (X30). Me teoric sparry calcite within a root mold. Bed 4a: Grains are tightly packed, and the amount of pore-filling sparite is sparse. Lack of dolomite is shown in Figure 13. Figure 13. Bed 4a, Titan Yellow staining (X20). Note lack of significant high-Mg calcite or dolomite, which would be stained red. White mass appears to be weathered shell fragment. Some phosphorite grains. 29
Bed 5a: Sparse high-Mg calcite or dolomite is present, typically associated with mollusk fragments. Abundant root molds are present, almost uniformly filled with a drusy mosaic pore filling cement (Fig. 14). Figure 14. Bed 5a, Alizarin Red S stain (X10). Meteoric sparry calcite in a root mold. Bed 6a: Some High-Mg calcite or dolom ite is present, typically associated with mollusk fragments (Fig. 16). A bundant root molds, almost uniformly filled with drusy mosaic pore filling cement (Fig. 17). Smaller pores are not completely filled with sparite. Figure 15. Bed 6a, Titan Yellow staining (X30). Meteoric sparry calcite precipitated within a dissolution cavity. Dolomitization near shel l debris is indicated by the arrows. 30
Figure 16. Bed 6a, etched (X70). Meteoric sparry calcite precipitated within a dissolution cavity. The cement that binds the packstone appears to consist of two di stinct types. The more abundant is an interstitial micrite com posed of low-Mg calcite. This micrite fills most of the original interstitial space a nd likely formed due to the alteration of preexisting aragonitic grains (Per kins, 1977; Scott, 1997). Blocky cement, drusy-mosaic cement, circ umgranular sparry calcite, and calcite crystals with a dogtooth habit ar e all indicative of a meteoric vadose or meteoric phreatic diagenetic environments (Longman, 1980; Fl gel, 2004). Low-Mg calcite is very strongly associated with a freshwater (non-marine) origin (Land, 1970; Folk, 1973; Flgel, 2004). Additionally, paleokarst can be recognized by the presence of vadose cements (Wright, 1982). 31
32 Thus, the morphology of calcite crystals as well as the mineralogy and fabric of the sparry calcite cement all indicate a period of exposure to meteoric waters. Additionally, karstic dissolution, development of secondary porosity, and root molds are present in each of the packstone beds, furthe r indicating periods of subaerial exposure. Because the overlying and underlying shell beds show no significant signs of any of these processes, each of the packstone beds was subaerially exposed befo re being buried by the overlying shell bed. The presence of interstiti al micrite, exclusive to the packstone beds, appears to be related to the presence of me teoric sparry calcite cement and thus the formation of packstone. If the packstone beds formed in the vadose zone, then the boundary between the lower surface of each packstone bed and the immediately underlying shell bed may represent the aver age level of the water table following deposition of an individual unit. The original fabric and lithology of the packstone beds appears to have been similar to the underlying shell beds; a fi neto medium-grained quartz and carbonate packstone with abundant fossil material. However, post-depositional dissolution, micritization, and cementation by sparite have partially obscured the original similarity between the shell beds and the packstones. Water Depth During Deposition of Shell Beds A grain-size analysis was performed to identify possible tren ds in water depth between the depositional intervals. A coarse ning upward trend is typical of a shallowing upward series; a fining upward trend is conve rsely indicative of a deepening series. Grain size was measured using the following method, adapted from Griffiths (1967) and
Selley (2000). A sample weighing approxima tely 100 g was gathered from one of the stratigraphically-continu ous bulk samples for each bed. Particles larger than -1 dominantly consisting of shell material ha d previously been removed, so the analysis only focused on sediments within the clay to sand range. Prior to analysis, the samples were then oven-dried at approximately 50 C for eight hours. After drying, the samples were weighed to the nearest 0.01 g and placed at the top of a series of sieves sized at -1 0 1 2 3 and 4 Each set of sieves was agitated using a Ro-Tap for fifteen minutes. The residu e in each sieve was weighed and the sieves were cleaned between each sample. The fine fraction in the catch tray, i.e., sediment < 4 was analyzed using a Malvern laser diffractometer. Cumulative Grain Sizes for Lower Portions of Shell Beds0% 10% 20% 30% 40% 50% 60% 70% 80% 90% 100% 1211109876543210-1 PhiPercentage 6c 5c 4c 3c 2c 1a Figure 17. Cumulative grain sizes for lower portions of shell beds. 33
34 Detailed results of the grain size analysis are provided in Appendix B. Figure 17 shows a summary of the results. The grai ns are very well sorted and are composed almost exclusively of size 2 to 3 particles: medium to fi ne sand. The silt and clay fraction is negligible but present. This sor ting pattern is typical of tidal or beach-type environments (Visher, 1969; Davis, 1994a), hardly surprising in light of the nature of the deposit or the faunal assemblage. A non-quantitative analysis of the sand-, silt-, and clay-sized sedi ment in the shell beds was performed by adding 2 M HCl to the sieved residue until all carbonate material dissolved. A visual estimate of post-dissolu tion volume showed that at least 50 % of the sediment in size ranges 0 to 4 remained and is therefore non-carbonate. The key trend, however, is that there is an upward increase in the relatively coarse fraction between shell beds. There is a pr onounced shift from fine sand to medium and coarse sands between the lower shell beds (5 a nd 6) and the upper shell beds (1 and 2). A coarsening upward trend is indicative of th e slow encroachment of an increasingly higher-energy (i.e., shallower) depositional environment (Prothero and Schwab, 1996; Posamentier and Allen, 1999). Therefore, this series of deposits ap pears to represent a vertically stacked seri es of near-shore marine deposits th at were deposited at increasingly shallow water depths. Bivalve and Gastropod Analysis Existing bivalve and gastropod faunal lists (C helladurai et al., 2006; Greene et al., 2006) of the LL shell beds were verified and enhanced by comparison with bulk samples and sorted collections from the LL shell beds. Gastropods were listed as either present or
35 absent from the section as a whole and were, as previously discussed, used primarily to verify that the section was part of the Bermont fauna (DuBar, 1962; DuBar, 1974). Bivalves species abundance by shell bed was recorded, then depth information was compiled from the Malacolog database (R osenberg, 2005) and l iterature (Abbott et al., 1995; Redfern, 2001). Bivalves were used to verify the sections placement in the Bermont formation as well as to estimate the water depth at which the biota that formed the shell beds resided. Such an estimate would provide an approximate depth of formation of the shell beds pr ovided that transport was rela tively limited. A weighted average of minimum and maxi mum depth was calculated in corporating all species for which a depth was available in the literature. Species for which no depth information was available were disregarde d; this amounted to 19 species out of 97 total; 14 of these species were represented by three or fewer specimens out of a total sample of 13,793. Details of the bivalve assemblage analysis are provided in Appendix C. Table 1 shows a summary of the results of a weighted average analysis. The average minimum water depth in which the bivalve fauna of the shell beds lived was 4 2 m. A total of 41 of the 78 species have maximum depths le ss than 13 m; these species represent 12,125 specimens of 13,793 total, or 88.9 % of the bi valve population. By comparison, only 4 of 78 species had minimum depths that were grea ter than 13 m; these species represent 64 specimens of 13,793, or 0.5% of the bivalve pop ulation. The deep-water specimens may have been transported into shallower wa ters (< 13 m) by taphonomic processes; alternately, the currently known minimum range is incorrect. There is no minimum depth trend; all beds fall within the first standard deviation. The water depth range of the bivalve taxa is 2 m to 13 m, with in a 90 % confidence
36 interval; the mean of this ra nge, 7.5 m, will be used in subs equent calculations of sea level. Bed 6b is shallower than th e other beds due to an abundance of Chione elevata, which has a minimum depth of 0.6 m. The majority of the bivalves were not articulated and showed damage and wear indicative of local transport; thus, the bivalve depth ranges provide an estimate of the overall depth during the deposition of the shell beds, rather than the precise depth at any specific instant. Table 1. Weighted Average Minimum Bivalve Depth for Longan Lakes Shell Beds. Weighted Average Minimum Bivalve Depth for Longan Lakes Shell Beds Bed n Weighted Minimum Depth (m) 2c 2649 5 3c 1504 5 4c 2592 6 5c 3280 4 6b 3571 2 However, Anodontia alba found in life position at th e tops of beds 2, 3, and 4, occurs exclusively in shallow water, with a listed live depth range of 1 m (Abbott et al., 1995; Rosenberg, 2005). If the presence of Anodontia alba in life-position is a reliable indicator of the water depth of the underlying shell material, this constrains the water depth to 1 m and would change the sea-level calculations undertaken later in the study.
37 Chapter Five Models of Sea-Level Change Models not involving transgression that can account for marine deposits overlying freshwater or subaerial deposits are unlikely to occur in tectonical ly stable southern Florida (Smith and Lord, 1997). Additionally, southern Florida is not proximal to a siliciclastic sediment source capable of overwhelming the eustatic signal (White, 1970; Roof et al., 1991) nor are any the sediments comprising the units dominated by silicilastics. Eustatic change s should therefore necessarily im pact Floridas coastline in a relatively straightforward manner. If eustatic sea level rises, Floridas coastline should retreat; if eustatic sea level falls, Floridas coastline should prograde i.e., the Florida Platform is therefore an excelle nt sea-level dip stick. Sequence Stratigraphy Because the age of Floridas early Pleisto cene shell beds is difficult to constrain, the strata are chronostratigraphically ambi guous. This chronological ambiguity is additionally problematic when a sequence stra tigraphic model is applied. The marine flooding surfaces and erosional unconformities that delineate parasequence and sequence boundaries, respectively, are present, but correlation of such boundaries between different locations is diffi cult, if not impossible.
38 Floridas Miocene and Pliocene sequence st ratigraphy has been studied in some detail (Evans, 1989; Evans and Hine, 1991; Mallinson and Compton, 1995; Cunningham et al., 1998), but Pleistocene de posits have received only cursor y attention, typically as a footnote in studies of older sections (Perkins, 1977; Zullo and Harris, 1992; Harris and Zullo, 1993; Warzeski et al., 1996; Cunningha m et al., 2001; Cunningham et al., 2005). As a result, the impacts of Miocene and P liocene eustatic change s on the south Florida platform stratigraphy are better known th an more recent Pleistocene changes. Although the identification of unconformities and their correlative conformities in deeper marine settings is one of the key crit eria used to distinguish sequence stratigraphic units (Van Wagoner et al., 1988) the technique is difficult to apply in locations: 1) represented by chronologically ambiguous vertical sequences which obscure the differences between sequence and parase quence boundaries; 2) with lithologic homogeneity that confounds meaningful late ral correlation; and 3) in regions with discontinuous lateral beds, t hus preventing the ready appli cation of Walthers law of correlation of facies. Floridas Pleistocene sh ell beds represent all three of these potential shortcomings, and these make sea-level rec onstruction difficult. Cyclostratigraphic techniques are similarly difficu lt to apply but are instead ha mpered primarily by the lack of high-resolution numerical dating of Fl oridas Plio-Pleistocene record. Cyclostratigraphy Because the tools of sequence stra tigraphy (Van Wagoner et al., 1988; Van Wagoner et al., 1990), as discus sed earlier, suffer from a number of limitations, a different method to model the origins of the strata at LL would likely be more
39 informative. At first glance, cyclostratig raphy seems suited for this type of data. However, cyclostratigraphic methods have tw o major requirements: 1) the cycles must represent equal intervals of time; and 2) the duration of the interval must be known (Schwarzacher, 1993). The LL strata fail to meet either of these requirements. To detect cycles that are missing from a sequence, Goldhammer, et al. (1990; 1993) developed a method to detect the presence of missed beats. However, their model produces useful results only with long sections ( over 700 m in both the 1990 and 1993 studies) that contain thirdthrough sixthorder cycles. An attempt by Goldhammer et al. (1990; 1993) to model fi ve Florida Pleistocene marine subtidal units from the Florida Keys previously descri bed by Perkins (1977) met with limited success; the model showed a 67,000 yr periodicity, which is not in tune with any known orbital forcing mechanism (Goldhammer et al., 1990; Joyce, 1990; Berger and Loutre, 1991). They concluded that this anomalous frequency was a consequence of missed beats. In short, the set of beds at LL is too limited stratigr aphically, too poorly constrained temporally, and contains too few cycles to analyze with cyclostratigraphic t echniques; missing beds within the LL strata cannot be identified. Table 2. Duration of Sea-Level Cycle Orders. After Kerans and Tinker (1997), Emery and Myers (1996), Posamentier and Allen (1999), Coe et al. (2003), Van Wagoner (1990), Vail et al. (1991), and Schlager (2005). Duration of Sea-Level Cycle Orders Cycle Order Duration Terminology Cause First > 50 Myr Tectono-eustasy Second 3 50 Myr Supersequence Tectonic subsidence Third 0.5 3 Myr Sequence Tectono-glacioeustasy Fourth 0.08 0.5 Myr Parasequence set Glacio-eustasy Fifth 0.03 0.08 Myr Parasequence Glacio-eustasy Sixth 0.01 0.03 Myr Glacio-eustasy
40 As cyclostratigraphy is no panacea, the imperfect but robust methods of sequence stratigraphy will be used to help determine the relationship between sea-level fluctuations and the Bermont strata. Table 2 displays the cycle orders and the inferred causes of that order of cycle. Third-order deposits are refe rred to as sequences (Coe, 2003) and form the fundamental unit of sequence stratigraphy (Kerans and Tinker, 1997). Fourth-order deposits are referred to as parasequences sets (Van Wagoner et al., 1990), and fifth-order deposits are parasequences (Vail et al., 1991; Kerans and Tinker, 1997; Schlager, 2005). Orbital Forcing by Obliquity Because the 41 kyr frequency was the dominant periodicity during the deposition of the early Pleistocene (J oyce, 1990), the likely interval for Bermont formation deposition, the most parsimonious value for th e time interval between the parasequence cyclothems, provided there are no skipped beats, is 41 kyr. This frequency represents variation in Earths obliquity cycle and its concomitant impact on solar insolation and ultimately on the Earths climate (Schwarzacher, 1993). Therefore, based on the inferred developm ent times for the packstone beds, which will be discussed below, and the dominant orbi tal forcing periodicity, the LL strata most likely represent fifth-order cycles superi mposed on a longer fourth-order cycle and should be therefore termed parasequences.
41 Fischer Plots and the Relationship Between Time and Cycle Thickness Fischer plots (Sadler et al., 1993) are used to analyze cycle thinning and thickening patterns, normalized to a uniform rate of subsidence (Read and Goldhammer, 1988; Kerans and Tinker, 1997). Table 3 shows the values that were used to construct the Fischer plot; the thickness of each individual interval, the averaged thickness of all the intervals, and the subsidence rate (6 m). A Fischer plot of the LL intervals, illustrated in Figure 18, was constructed. The single peak of the Fischer curve indicates that the deposition took place during a single lower-order, sea-level cycl e (Kerans and Tinker, 1997). As was shown earlier, the lower-order cyclicity shown on the pl ot is most likely fourth order and that each packstone bed marks the end of a shorter fifth-order cycle. Assuming sea-level highstands reached the same elevations, the thinning of cycles upward indicates that available accommodation space was being filled by deposits at a higher rate than it was being created by subsidence (Kerans and Tinker, 1997). At this point, it should be noted that Sadl er et al. (1993) favor a lower limit of 50 cycles per section in order to produce a Fischer plot that me rits interpretation because short sections suffer from the same problems as small sample a high standard deviation. Because Fischer plots innately force the st arting and ending points to be at the same horizontal position, small numbers of cycles of ten force specific interpretations. Because the LL strata only represent one cycle, as previously demonstrated, the range of interpretations is limited. Sadler (1993) recommend discarding the th ickest cycle to check the impact on the mean and standard deviation. Additionally th ey found that the standa rd deviation was 1/7
Table 3. Summary of Interv al Characteristics within the Longan Lakes Sequence. Summary of Interval Characteristic s within the Longan Lakes Sequence Unit Forming Top Bed of Cycle Upper Karst Bed (cm) Lower Shell Bed (cm) Net Thickness of Cycle (cm) Depositional Rate cm / kyr 2a 10 33 43 1 3a 10 56 66 2 4a 46 60 106 3 5a 50 60 110 3 6a 1 20 90 110 3 Total Thickness 168 247 415 Mean 27 52 81 2 Standard Deviation 19 13 32 1 1 Lower portion of cycle 6a is not included in calculations because of unknown thickness Subsidence Rate 6 m / Myr = 25 cm / 41k 25 cm Accumulation ( > Mean ) 42 Figure 18. Fischer plot for Longan Lakes strata. The Fischer plot is a graphical summary of combined effects of subsidence and cycle-specific sediment accumulation. The peaked curve indicates the presence of a single highstand, presumably 4 th -order, made up of four shorter 5 th -order segments. Increasing Time
43 of the cycle thickness when using a sample with at least 50 cycles. Applying this technique to the LL strata shows that the heig hts of the cycles change from 81 32 cm to 72 31 cm when the thickest parasequence is excluded. If that standa rd were applied to the LL mean cycle thickness of 81 cm, one would expect the standard deviation to be no greater than 22 cm. The standard deviation is 32 cm, approximately 50% higher than if a 50-cycle section had been used. Correlation of the LL Bermont Strata with a Eustatic Curve The amount of time that passed between the deposition of a shell beds and the underlying karstified packstone layers is uncertain; however, as was previously demonstrated, a reasonable estimate is 41 kyr because the primary orbital signature of the early Pleistocene epoch was obliquity. As will be shown below, the time required to form a shell bed and packstone interval falls within this time span. A complicating factor includes the fact that paleosols, often found at sequence boundaries, are not recognizable in the LL strata, having been eroded or otherwise removed (Selley, 2000). On a cautionary note, Drummond and Wilkinson (1993) concluded, using a computational model, that multiple cycles can develop during one highstand. For example, sea-level has fluctuated during th e Holocene highstand; sea-level stood at -9 m at 7.7 ka, rose to +2 m between 6.8 and 4.8 ka (Blum et al., 2001), dropped to -4 m at 3 ka (DePratter and Howard, 1981), and then rose to the present level. However, Drummond and Wilkinsons (1993) model postulates conditions of rapid sedimentation, limited accommodation space, and long duration of platform flooding, only the first of which is especially applicable to the LL site. Additionally, the
44 formation of packstone beds between the LL sh ell beds indicates that sufficient time was available to allow for cementa tion, dissolution, and micritization of the original shell beds prior to burial by the next shell bed. Flgel (2004) gives a range from 10 3 to 10 5 years as the time required for meteoric diagenesis to occur; shallow burial generally correlates with lower rates of diagenesis and deep burial with higher rates. Because the LL packstones were subaerially exposed, a rate of diagenesis in the lower half of Flgels range, from 10 3 to 10 4 kyr, will be used in subsequent discussion. To place the LL strata within existing eust atic curves, the lowstands represented by the packstone beds were correlated with s ea-level reconstructions based on variability in the 18 O record. The shape of the 18 O curve, shown in Figure 19, shows similar patterns of glaciation during the Bermont and late r Pleistocene; an interval of intensified glaciation followed by a slightly faster de glaciation (Joyce, 1990). However, the asymmetry in timing between interglacial and glacial intervals during the early Pleistocene, forced by the 41 kyr obliquity cy cle, appears to be less pronounced than the younger eccentricity-driven late Pleistocene gl aciation; glaciations appear to take only slightly longer than deglacia tions, and the differences in peaks and troughs of the curve are not as pronounced. Conversely, such an asymmetrical eustatic pattern would result in an interval of regression followed by a slightly more rapid transgression. In any event, the, shell beds would be subaerially exposed for 10 3 to 10 4 kyr, which coincides Flgels temporal estimates for near-surface diagenesis. A preliminary correlation of Floridas Plio-Pleistocene shell beds with third-order coastal-onlap cycles of an existing seque nce stratigraphic model for the Salisbury and
45 Albemarle embayments of Virginia and North Carolina was published by Zullo and Harris (1992) and Harris and Zullo (1993); in their model, the Bermont formation was assigned to the third-order sequence cycle 3.9 ; this cycle is bounded by ages of 0.8 and 1.6 Ma. Their placement of the Bermont into a sequence stratigraphic context, however, was based on an older Cenozoic coastal on lap chart published by Haq et al. (1987). A more recent reconstruction specific to the Plio-Pleistocene record in th e Gulf of Mexico (Wornardt and Vail, 1991) places this same interval in the third-order cycle 3.8. According to their Mio-Pleistocene Sequen ce Chronostratigraphy Chart, fourth-order sequence boundaries, which are indicative of lower sea level, occurred at 1.9, 1.4, and 1.1 Ma. Maximum flooding surfaces, indicative of sea-level high stands, are placed at 1.47, 1.3, and 0.92 Ma. A more recent revision of these dates (W ornardt, 1999) places the fourth-order sequence boundaries at 2.09, 1.56, and 1.40 Ma and maximum flooding surfaces at 1.59, 1.47, and 0.96 Ma; however, to date the majority of researchers continue to use the 1987 and 1991 values (Cunningham et al., 1998; Cunningham et al., 2001; Duncan et al., 2003; Le Roux et al., 2004). This study will use the sequence boundary and maximum flooding surface values published in 1987 and 1991 because they are widely accepted and were developed specifically for the Gulf of Me xico; the newer ages were derived from European basins and are less likely to be reflective of conditions in the Gulf of Mexico. If the newer values were used, the ages di scussed below would be approximately 100 kyr younger, still within the potenti al age range of the Bermont as delimited by Lyons (1991).
A eustatic curve, drawn after Haq et al (1987), is depicted in Figure 19. As discussed earlier in this st udy, the highstand value at 1.2 Ma represents a sea level between 10 m and 20 m above modern levels. There were two peri ods of transgression and highstand during the early Pleistocene, as well as two periods of sea-level fall. These relationships are shown in Table 4 and Fi gure 19. Haq et al. (1987) show the 1.4 Ma lowstand which separates the two highstands as having a duration of 50 to 100 kyr. 46 Figure 19. Bermont-age eustatic fluctuations correlated with Longan Lakes strata. LL strata are correlated with eustatic highstan d between 1.1 and 1.3 Ma and the 18O curve; packstone beds form during periods of lower sea level/increased ice volume. Figu re incorporates data from Lyons (1991), Wornardt and Vail (1991), Mix et al.(1995a; 1995b), and Allmon et al. (1996).
47 As previously discussed, the Bermont fo rmation was most likely deposited as a number of fifth-order paraseque nces that resemble cyclothems The LL strata consists of five parasequences of shell beds capped by subaerially exposed p ackstones, labeled 6, 5, 4, 3, and 2. Because the top of parasequence 1 was not observed, this bed will not be included in subsequent sea-le vel or temporal calculations. Table 4. Summary of Early Pleisto cene Interval Characteristics. Only highstand deposits are recorded in Florida; other portions are missing. After Van Wagoner et al. (1988), Wornardt and Vail (1991), and Wornardt (1999). Summary of Early Pleistocene Interval Characteristics Period Eustatic activity Expected Systems Tract 1.40 0.96 Sea level rise and highstand Tr ansgressive/ highstand sequence tract 1.47 1.40 Sea level fall Lowstand systems tract 1.56 1.47 Sea level rise and highstand Tr ansgressive/ highstand sequence tract 1.59 1.56 Sea level fall Lowstand systems tract The previously discussed consistent upward coarsening pattern of grain size provides evidence of a shallowing upward series of shell beds. If a major (e.g., fourthorder) lowstand with a duration of 100 kyr interr upted the LL strata, it is unlikely that deposition would recommence w ithout signs of a significant unconformity. Such an unconformity might be indicated by the presence of paleosol s, a change in grain-size counter to the existing coarseni ng upwards trend, karstification of the existing strata, or a shift in fauna indicating a change in water de pth. Because none of these indicators are present to any significant degree at the unconfor mities located at th e upper surface of the packstones, it will be assumed that the strata were not inte rrupted by a 100 kyr lowstand. Thus, if a 41-kyr control by obliquity is the primary forcing mechanism, consistent with the 18 O record, at least approximately 160 kyr must have passed between
48 the development of the lower and uppermost subaerial exposure beds. As shown in Table 4 and in Figure 19, if Wornardt and Vails (1991) eustatic curv e is correct, then there are two periods of transgression and highstand th at are coeval with the age Lyons (1990) designated for the Bermont. As previously shown in this study, the LL Bermont strata were most likely deposited during a period of fourth-order highstand. The older interval, from 1.60 Ma to 1.45 Ma, had a duration of less than 150 kyr; the younger interval spanned from 1.35 Ma to 1.1 Ma. Highstand sy stems tracts are depos ited during periods when the relative rate of sea-level rise decel erates (Emery and Myers, 1996); according to Wornardt and Vails (1991) eustatic curve, the younger highstand interval took place between 1.3 Ma and 1.1 Ma. Therefore, the LL Bermont strata were likely deposited during the younger interval. Because the volume of ice sheets can be estimated using the 18 O of benthic foraminifera as a proxy (Mix et al., 1995a; Hoefs, 2004), an approximation of sea level can be calculated (Fairbanks, 1989). As the ice volume decreases, sea level rises and the relative proportion of 18 O in the ocean decreases. A lthough a quantitative correlation of the shell beds with existing 18 O curves is beyond the scope of this study, a possible qualitative correlation which as signs shell bed intervals to sea level highstands between 1.3 and 1.1 Ma is depicted on Figure 19. Using Pleistocene corals from Barbados, Fairbanks and Matthews (1978) calculated that a sea level rise of 1 m would occur for every of 0.011 reduction in 18 O. However, this value is specifically linked to the last glaciation (H oefs, 2004) and assumes that all changes in 18 O are linked to ice volume. There could also be temperature effects that are superimposed upon the changes in 18 O forced by ice-volume fluctuations.
49 Therefore, using the 0.011/m relations hip to calculate earlier sea-level fluctuations will result in an approximation that most likely overestimates the actual amount of changes. In any event, if the 0.011/m relationship is reflective of the interval between 1.1 Ma and 1.6 Ma, the average range of sea-level fluctuations during the early Pleistocene would have been approximately 110 meters. This value was calculated from the 18 O smoothed curve in Figure 19. An additional consequence of the time of deposition relates to the inferred subsidence rate, 6 m/Ma. Approximately 1 m of subsidence took place over the 160 kyr interval that most likely represents the time required to form the LL strata. The measured height of the parasequences (6 a to 2a) is 3.4 m. The mean depth determined by the use of bivalve depth ranges, as previously demons trated, was 7.5 m. Therefore, in order encompass both the mean bivalve depth of th e shell beds and the subaerially exposed packstones, the amplitude of the fifth-order, sea-level fluctuations must have exceeded approximately 10 m (7.5 m + 3.4 m height of strata 1 m of s ubsidence). This is at the lower end of estimates of fifth-order sea-leve l fluctuations, which range from 1 m to 150 m (Kerans and Tinker, 1997). Impacts of Uplift and Subsidence Absolute elevation changes of the depositional environment relative to the geoid are a factor that must be considered. The causal mechanisms can include karstic collapse, uplift induced by karstification of overburde n, and subsidence. Compared to activemargin regions, such as Barbados and Papua-New Guinea, where changes in Quaternary sea level have been investigated (Chappe ll, 1974; Fairbanks, 1989; Chappell and Polach,
50 1991), subsidence and uplift is not a major fact or in southern peninsular Florida. However, considering the comparatively small thickness of the sections, even relatively small amounts of change in the platforms elevation could impact the stratigraphic signature. Previous studies typically assume that the Florida platform is stable (Denizman and Randazzo, 2000) and ignore subsidence and uplift. Reductions in the mass of overbur den by erosion or dissolution (e.g. karstification) can lead to isostatic uplift, particularly in areas with abundant karst and major springs; calculated rates of loss of el evation of limestone due to dissolution (1 m limestone/38 ka) and the corresponding isos tatic uplift in response to the loss of limestone (1 m/41 ka) are approximately equal (Opdyke et al., 1984), leading to no significant net change in elev ation. However, this uplift phenomenon appears to be restricted to the karst-rich northern portion of the Florida Peninsul a (Opdyke et al., 1984). The LL overburden is 5.5 m thick and com posed primarily of sands with some fossil material. These sediments lack any i ndication of karstification and is sufficiently thin so that it should not be a factor in potential uplif t. Additionally, because the elevation of the modern surface is 5 m above sea-level and the post-Bermont highstand was approximately 10 m above modern sealevel (DuBar, 1974; Wornardt and Vail, 1991), the mass of potentially absent overburden material (i.e., material that may have been deposited during the post-Be rmont highstand and that has since eroded) is less than 5 m. Thus, the potential loss of overburden is unlikely to have caused uplift at LL. Furthermore, as previously discussed, ther e was not evidence of karstification in the LL Bermont strata beyond an early merokarst.
51 Modeling Early Pleistocene Sea Levels with the Bermont Strata Given the age assigned to the Bermont of 1.1 Ma to 1.6 Ma (Lyons, 1991), the 6 m/Ma subsidence rate yields a range of Berm ont-age subsidence relative to the present day elevations from 6.6 m for younger strata to 9.6 m for older strata, with a mean of 8.1 m. As a result, the LL Bermont sequence shoul d be located an average of 8.1 m below its original elevation of deposition. Because th e numerical age of the beds is not known, the mean will be used in subsequent calculations of Bermont age sea-level stands. Adding this correction of 8.1 m to the surveyed depth relative to modern mean sea level (mmsl) of the karst beds gives a he ight of 3.7 m (-4.4 + 8.1) above mmsl for the lowermost packstone bed 6a and a height of 6.9 m (-1.2 + 8.1) above mmsl for uppermost packstone bed 2a. The mean height of thes e packstone beds is 5.3 m above mmsl. As previously discussed, the bivalv e taxa indicate that the average water depth was 7.5 m. Therefore, the sea-level pos ition, most likely representing peak highstand, during the formation of the unit was most likely an av erage of 12.8 m above the modern mean sea level, with a possible range from 11.2 m to 14.4 m. These relationships are summarized in Figure 20. A representative reconstruc tion of this sea level, based on modern elevations, is shown in Figure 4. The key point is that sea levels during th is period were higher than modern sea level. The value of 12.8 m above the modern mean sea level compares favorably with existing estimates of early Pleistocene sea leve ls. By synthesizing a variety of sources, Haq et al. (1987) calculate a highstand between 10 m a nd 20 m above mmsl between 1.1 Myr and 1.5 Myr. Based on paleoecol ogical and topographic data, Dubar (1974) assigned a maximum sea level of + 50 f eet (15 m) to the Bermont formation.
Malmgren and Berggren (1987) calculated a eustatic highstand approximately 15 m above mmsl during the ea rly Pleistocene using 18 O of benthic foraminifera. Figure 20. Spatial relations of the Bermont formation at Longan Lakes. The early Pleistocene sea-level is the sum of the current elevation, the paleod epth, minus the subsidence (which adds because it is negative). Thus, the early Pleistocene sea level wa s approximately 13 m above the modern sea level. 52
However, if the previously di scussed presence of in situ Anodontia alba is a more reliable indicator of a water depth than th e average minimum depth of the most common taxa, then the sea level stand would instead on ly be 6.3 m above mmsl. If this lower sea level highstand is accurate, then it indicates th at previous estimates of early Pleistocene msl are too high. A representative reconstruc tion of this sea level, based on modern elevations, is shown in Figure 21. Figure 21. + 6.3 m Pleistocene high sea level based on Anodontia alba (1.2 Ma). 53
54 Chapter Six Conclusions The early Pleistocene Bermont strata at Longan Lakes preserve extraordinarily unambiguous indicators of sea level fluctuations; a 6-m cyclothem-type set of beds consisting of six marine shell beds with five interbedded, diagenetically produced, packstone beds. The repetitive nature of the LL Bermont strata allows for additional tuning of Floridas sequence stratigraphic model and suppor ts the hypothesis that the Bermont formation belongs within sequence cycle 3.8. The oxygen isotope record (Joyce, 1990; Mix et al., 1995a; Mix et al., 1995b) shows that frequent low-amplitude eustatic change dominates the sea-level record during the early Pleistocene; the LL Bermont strata provide strong circumstantial evidence that these rapid eustatic changes affected south Floridas lower Pleist ocene stratigraphy. The strata indicate that early Pl eistocene sea-levels fluctuated a minimum of 10 m between highstands and lowstands. The Bermont stra ta also provide evidence that supports a series of early Pleistocene eustatic highstands between + 6 m and + 13 m above Recent sea-levels. Furthermore, south Floridas 6 m/Myr subsidence rate, low but measurable, allows for preservation of strata that woul d otherwise be reworked during transgressive cycles across the low-gradient carbonate platform. This study also indicates th at it is likely that the Be rmont strata at LL were deposited between approximately 1.3 and 1.1 Ma based on correlation with the sea-level
55 curve of Haq et al. (1987). Verification by better-constrained chr onostratigraphic data between individual beds at LL will provide i ndependent verification of the results and will allow further tuning of the model. Finally, this study shows that it is lik ely that the deposits of the Bermont formation record an interval of at least 160 kyr du ring the early Pleistocene. The faunal package that identifies the assemblage theref ore persisted for a significant amount of time and is consequently important to studies of Floridas early Pleistocene, particularly paleoecological studies that i nvestigate the impact of sea le vel changes on marine fauna. Previous studies have shown relationship s between sea level and species richness (Harries, 2003) as well as the independence of species richness from sea level (Valentine and Jablonski, 1991); the LL strata, a record of multiple highstand intervals, provide a ready-made workshop to study the effects of repetitive sea level changes on early Pleistocene fauna.
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71 Appendix A: Lithologic Data Descriptions of the individual beds each contain descriptions of the lithology and an overview of the biota. Bed 1b 453-505 Moderately sorted silt to fine creamy wh ite sands. Poorly defined fining upwards of grains. Over 50% bioclast material cons isting of medium to sm all-cobble sized shells and shell fragments. No major preferred orientation, over 25% of shells are concave downward. Some coral fragments ( Manicina sp. ) are present. Fossils include Anadontia sp ., Chione elevata Turritella Lucinidae, and Pectinidae. Some Tellinidae are still articulated. Some Anadontia sp. are present in life position. Some Chione elevata are still articulated. Bed 1c 435-453 Poorly sorted silt to cobble size white sediment and shelly bioclast material. Sediments fine upwards into Bed 1b. Over 75% bioclast material consists of medium to cobble sized shells and shell fragments. Some preference in position of shells is displayed, with over 25% of shells lying concave upward. Rare (< 1%) signs of predatory gastropod boring. Fewer than 10% of bivalves are articulated. Shelly material includes Veneridae ( Chione elevata ), Turritella Lucinidae, Pectinidae, and Conus sp Over 50% of shells are Chione elevata Some Tellinidae are still articulated. Some Anadontia sp. are present in life position. Some Chione elevata are still articulated. Also noted Busycon spiratum (up to 9 cm), Anomia sp ., Ostreidae, and Crepidula sp
72 Appendix A (Continued) Bed 2a 425-435 Moderately sorted fine tan cemented sa nd and some shelly bioclast material classified as a packstone. Visible signs of weathering (e.g. vugs). Approximately 75% of shells are fragmented. Vert ical breaks approximately 10 cm wide penetrate through Bed 2a every 1 to 2 meters allow sediments to pe netrate from Bed 1c to Bed 2b. Freshwater gastropods (Planorbidae) pres ent near top of bed. Bed 2b 415-425 Dark grey to brown fossiliferous to sparsely fossiliferous packed biosparite, crystallized/lithified around sand to pebble si zed bioclasts. Boring and burrowing traces (< 25%) are present. Very fine white sand is lodged between cracks and voids in the rock. Unit thickness ranges from 10 cm to 20 cm. Up per bedding plane is burrowed and pitted. Cracks in rock (approximately one 10 cm break every 1 to 2 meters) allow collapse and intrusion of material from Bed 1c. Br yozoan encrustation and trace yellow carbonate crystallization present within vo id cavities. Bioclasts include Chione elevata Diodora sp., and Olividae. Wavy contact with Bed 2c fluc tuates over 15 cm vertically Bed 2c 392-415 Poorly sorted silt to cobble size white sediment and shelly bioclast material. Over 60% bioclast material consists of medium to cobble sized shells and shell fragments. Over 60% of disarticulated shells are concave upward. Sediments fine upwards in upper 5
73 Appendix A (Continued) cm of bed. Rare (< 1%) signs of predat ory boring, less than 10% of bivalves are articulated. Shelly material includes Veneridae ( Chione elevata ), Turritella Lucinidae, and Pectinidae. Some Tellinid ae are still articulated. Some Anadontia sp. are present in life position. Some Chione elevata are still articulated. Also noted Busycon spiratum (up to 9cm), Anomia sp., Ostreidae, and Crepidula sp Abrupt contact, bottom of Be d 2c undulates 5 cm vertically over a 2 meter lateral distance. Bed 3a 382-392 Dark grey to brown fossiliferous to sparsely fossiliferous micrite, crystallized/lithified around pebble sized bioc lasts and classified as a packstone. Boring and burrowing traces (< 25%) are presen t. Very fine sand is lodged between cracks and voids in the rock. Unit is 10 to 20 cm thick. Bioclasts include Chione elevata Diodora sp ., and Olividae. Bryozoan encrustation a nd trace yellow carbonate crystallization present within void cavities. Abrupt contact, bottom of Bed 3a undulates 3 cm vertically over 2 meter lateral distance. Bed 3b 345-382 Moderately sorted silt to fine creamy wh ite sands. Over 40% bioclast material consisting of medium to small cobble sized sh ells and shell fragments. Fining upwards
74 Appendix A (Continued) but bioclast content up to 70% at top of bed. No major pref erred orientation, over 25% of shells are concave downw ard. Fossils include Chione elevata Turritella Brachiodontes sp ., Conus sp. Lucinidae, and Pectinidae. Some Te llinidae are still articulated. Some Anadontia sp. are present in life position. Some Chione elevata are still articulated. Some coral fragments ( Manicina sp. ) present. Gradual, diffuse contact with over 5 cm relief. Bed 3c 326-345 Poorly sorted silt to cobble size white sediment and shelly bioclast material. Over 60% bioclast material consisting of medium to cobble sized shells and shell fragments. No major preferred orientation, over 25% of shells are concave downward. Sediments fine upwards in upper 5 cm of bed. Rare (< 1%) signs of predator y boring, less than 10% of bivalves are articulated. She lly material includes Veneridae ( Chione elevata ), Turritella Lucinidae, and Pectinidae. Some Te llinidae are still articulated. Some Anadontia sp. are present in life position. Some Chione elevata are still articulated. Also noted Busycon spiratum (up to 9cm), Anomia sp ., Ostreidae, and Crepidula sp Wavy contact, top of Bed 4a weathered, contains boreholes and burrows with relief up to 25 cm.
75 Appendix A (Continued) Bed 4a 280-326 Moderately sorted silt to fine creamy white sands. Grains are cemented with scattered friable areas that have a higher con centration of bioclastic debris, all classified as a packstone. Over 40% bioclast material consisting of medium to small cobble sized shells and shell fragments. Fining upwards. No major preferred orientation, over 25% of shells are concave downw ard. Fossils include Chione elevata Turritella Lucinidae, and Pectinidae. Some Tellinidae ar e still articulated. Some Chione elevata are still articulated. Some coral fragments ( Manicina sp .) present. Bed 4b 250-280 Moderately sorted silt to fine creamy wh ite sands. Over 40% bioclast material consisting of medium to small cobble sized sh ells and shell fragments. Fining upwards. No major preferred orientation, over 25% of shells are concave downward. Fossils include Chione elevata Turritella Lucinidae, and Pectinidae. Some Tellinidae are still articulated. Some Anadontia sp. is present in life position. Some Chione elevata are still articulated. Some coral fragments ( Manicina sp. ) present. Bed 4c 220-250 Poorly sorted silt to fine creamy white sands. Over 60% bioclast material consisting of medium to cobble sized shells and shell fragments. Fining upwards. No major preferred orientation, over 25% of she lls are concave downward. Fossils include Chione elevata Conus sp., Turritella Lucinidae, and Pectinidae. Some Tellinidae are still articulated. Some Anadontia sp. is present in li fe position. Some Chione elevata are still articulated.
76 Appendix A (Continued) Flat linear contact with few dips. Bed 5a 170-220 Dark grey to brown fossiliferous to sparsely fossiliferous micrite, crystallized/lithified around pebble sized bioclasts and classified as a packstone. Very fine sand is lodged between cracks and voids in the rock. Bottom of bed has 10% burrows (mm scale) and rhizolith (root) traces consisting of primarily vertical cylindrical tubes (mm scale) containing wood fragments. Some oxidation present near base of bed. Boring and burrowing traces (< 25%) are present. Bioclasts include Chione elevate, Diodora sp., and Olividae. Bryozoan encrusta tion and trace yellow carbonate crystallization present within void cavities. Bed 5b 150-170 Silty sand, moderately well-sorted with sand to gravel size bivalve and gastropod shells and shell fragments. Coral fragment of Solenastrea hyades > 15 cm diameter embedded in sediment, visible traces of other 5 to 10 cm spheres. Bed 5c 110-150 Poorly sorted silty to fine creamy white sands. Over 60% bioclast material consisting of medium to cobble sized shells and shell fragments. Fining upwards. Over 25% of shells are concave upwards. Fossils include Chione elevata Turritella Lucinidae, and Pectinidae. Some Tellinidae are still articulated. Some Anadontia sp. are present in life position. Over 25 % of Chione elevata are still articulated.
77 Appendix A (Continued) Bed 6a 90-110 Dark grey to brown fossiliferous to sparsely fossiliferous micrite, crystallized/lithified around pebble sized biocla sts and classified as a packstone. Orange rust oxidation present on ove r half of material. Very fine sand is lodged between cracks and voids in the rock. Boring and burro wing traces (< 25%) ar e present. Bioclasts include Chione elevata Diodora sp., and Olividae. Bryozoan encrustation and trace yellow carbonate crystallization present within void cavities. Bed 6b 20-90 Poorly sorted silty to fine creamy white sands. Over 60% bioclast material consisting of medium to cobble sized shells a nd shell fragments. Over 25% of shells are concave upwards. Sediments co arsen upwards. Fossils include Chione elevata Turritella Lucinidae, and Pectinidae. Some Tellinidae are still articulated. Some Anadontia sp. are present in life position. Over 25 % of Chione elevata are still articulated. Bed 6c 0-20 Moderately well-sorted fine clayey-silty sand with fine gravel sized shells including bivalves, barn acles, and shell fragments. Fossils include Chione elevata Lucinidae, and Pectinidae.
Appendix B: Grain Size Data Table 5. Summar y of Grain Size Anal y sis. 78
79 Appendix B (Continued) Table 6. Sorting Coefficient by Bed. Bed Sorting Coefficient 6c 84 16 95 5 3 4 1 5 4 6.6 -0.25 -0.606060606 -0.856060606 5c 84 16 95 5 2 4 0 5 4 6.6 -0.5 -0.757575758 -1.257575758 4c 84 16 95 5 2 4 0 4 4 6.6 -0.5 -0.606060606 -1.106060606 3c 84 16 95 5 2 4 0 4 4 6.6 -0.5 -0.606060606 -1.106060606 2c 84 16 95 5 1 4 0 4 4 6.6 -0.75 -0.606060606 -1.356060606 1a 84 16 95 5 0 4 -1 4 4 6.6 -1 -0.757575758 -1.757575758
Appendix B (Continued) Cumulative Grain Sizes0.000000 0.100000 0.200000 0.300000 0.400000 0.500000 0.600000 0.700000 0.800000 0.900000 1.000000 1211109876543210-1 PhiPercentage 6c 5c 4c 3c 2c 1a Figure 22. Cumulative grain sizes. 80
Appendix B (Continued) Cumulative Grain Sizes0.00 0.10 0.20 0.30 0.40 0.50 0.60 0.70 0.80 0.90 1.00 1211109876543210-1 PhiPercentage 6c 5c 4c 3c 2c 1a Figure 23. Cumulative grain sizes. 81
Appendix C: Bivalve Data Table 7. Weighted Average Bivalve Dept h in Meters for Representative Beds from LL. 82
Appendix C (Continued) 83 Table 8. Wei g hted Avera g e Bivalve De p th p er C y cle.