AD T.M. 34 Geomorphology and Sediments | of the Inner Continental Shelf Palm Beach to Cape Kennedy, Florida by Edward P. Meisburger and David B. Duane TECHNICAL MEMORANDUM NO. 34 FEBRUARY 1971 U. S. ARMY, CORPS OF ENGINEERS COASTAL ENGINEERING ‘crag RESEARCH CENTER This document has been approved for public release and sale; its distribution is unlimited . Reprint or republication of any of this material shall give appropriate credit to the U. S. Army Coastal Engineering Research Center. Limited free distribution within the United States of single copies of this publication is made by: Coastal Engineering Research Center 5201 Little Falls Road, N.W. Washington, D. C. 20016 Contents of this report are not to be used for adver- tising, publication, or promotional purposes. Citation of trade names does not constitute an official endorsement or approval of the use of such commercial products. The findings in this report are not to be construed as an official Department of the Army position unless so designated by other authorized documents. TM LW wv 0030110001080 Geomorphology and Sediments of the Inner Continental Shelf Palm Beach to Cape Kennedy, Florida by Edward P. Meisburger and David B. Duane TECHNICAL MEMORANDUM NO. 34 FEBRUARY 1971 U. S. ARMY, CORPS OF ENGINEERS COASTAL ENGINEERING RESEARCH CENTER This document has been approved for public release and sale; its distribution is unlimited . ABSTRACT The Inner Continental Shelf off eastern Florida was surveyed by CERC to obtain information on bottom morphology and sediments, subbottom structure, and sand deposits suitable for restoration of nearby beaches. Primary survey data consists of seismic reflection profiles and sediment cores. This report covers that part of the survey area comprising the inner Shelf between Palm Beach and Cape Kennedy. Sediment on beaches adjacent to the study area consists of quartzose sand and shell fragments. Median size of midtide samples generally lies in the range between 0.3 to 0.5 mm (1.74 to 1.0 phi) diameter. The Shelf in the study area is a submerged sedimentary plain of low relief. Ridge-like shoals generally of medium-to-coarse (0.25 to 1.0 mn) calcareous sand resting on the seaward dipping subbottom strata contain material suitable for beach restoration. A minimum volume of 92.2 x 10° cubic yards of suitable sand is available within study limits. FOREWORD This report is the second of a series which will describe CERC's exploration of the Inner Continental Shelf. The program (ICONS) has the basic mission of finding offshore deposits of sand suitable for artificial beach restoration and nourishment. Edward P. Meisburger, staff geologist, and David B. Duane, Chief of the Geology Branch, prepared the report under the general supervision of George M. Watts, Chief of the Engineering Development Division. The field work was done by Alpine Geophysical Associates under contract (DA-08-123-CIVENG-65-57, modified). Cores taken during the exploration are stored at the Smithsonian Oceanographic Sorting Center (SOSC). Microfilms of the seismic profiles, the 1:80,000 navigational plots, and other associated data are at the National Oceanographic Data Center (NODC). Requests for information relative to these items should be directed to SOSC or NODC. Dr. Joseph Rosewater and Mr. Walter J. Byas of the Mollusk Division, Smithsonian Institution, verified the identification of the important biogenic constituents of the sediments. Their assistance is deeply appreciated. At the time of publication, Lieutenant Colonel Edward M. Willis was Director of CERC. NOTE: Comments on this publications are invited. Discussion will be published in the next issue of the CERC Bulletin. This report is published under authority of Public Law 166, 79th Congress, approved July 31, 1945, as supplemented by Public Law 172, 88th Congress, approved November 7, 1963. Section Section Section Section Section Il. Ill. TiVee CONTENTS INTRODUCTION . 1. Background . o ¢ 2. Field and letbarencerr proeoduces 3. Scope - . 4. Geologic seeeine 0 GEOMORPHOLOGY AND SHALLOW SUBBOTTOM STRUCTURE OF THE CONTINENTAL SHELF 1. Continental Shelf Geomorphology 2. Shallow Subbottom Structure CHARACTERISTICS OF SURFACE AND SHALLOW SUBBOTTOM SEDIMENTS OF THE CONTINENTAL SHELF . 1. General INTERPRETATION . 1. Sediment Distribution and Origin . 2. Sand Requirements 3. Suitability . 4. Potential Borrow Areas 0 SUMMARY LITERATURE CITED . APPENDIX A - Selected Geophysical Profiles . APPENDIX B - Granulometric Data APPENDIX C - Core Descriptions . Table I Stratigraphic Column: Upper-Eocene to Recent: Palm Beach, Florida, Coastal Zone . II Constituents most Commonly Found in Coarse Fraction - Fort ILLUSTRATIONS Pierce Sediments III Fill Requirements for Martin County, and Brevard County South of Canaveral Harbor Inlet . Cape Kennedy- Page ro BBNF 13 13 17 29 29 43 43 49 51 54 67 69 73 79 86 30 50 Figure 10 11 12 13 14 ILLUSTRATIONS (Continued) General Map of the Study Area . Navigation Plot Showing Survey Tracklines and Core Locations, Fort Pierce Grid Area Navigation Plot Showing Survey Tracklines and Core Locations in Reconnaissance Areas North (left) and South (right of Fort Pierce Grid Schematic Profile of Shelf Morphology Typical of the Study Area and Descriptive Terminology : Map Showing the Major Morphologic Features of the Continental Shelf in the Study Area . Section of a Dual Channel Seismic Reflection Record Obtained in the Study Area Schematic Profile Showing Characteristics of Prominent Shallow Acoustic Reflectors Underlying the Bottom . Contour Map of the Surface of the Blue Acoustic Reflector The Isopachous Map of the Interval from the Water- Sediment Interface to the Top of the Shallow Blue INCOSE IN QeeCre 5 66 G6 0 0 5 6 a6 Contour Map of the Surface of the Yellow Reflecting Horizon, Depths are in feet below MSL.. 990 Contour Map of the Surface of the Orange Reflecting Horizon. Depths are in feet below MSL. 0 © Contour and Isopach Maps of the Blue Reflector in the Fort Pierce-Canaveral Bight Reconnaissance Area. Depths are in feet below MSL. Contour and Isopach Maps of the Surface of the Blue Reflector in the Reconnaissance Area between Fort Pierce and Palm Beach. Depths are in feet below MSL . Exterior and Interior Views of Valves of Pelecypods Commonly Found in Whole or Gragmented Sediments from the Study Area Page 14 1S 18 20 21 22 23 25 27 28 31 Figure 15 16. 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 ILLUSTRATIONS (Continued) Views of Pelecypod and Skeletal Fragments of other Organisms which are Prominent Constituents of Sediment from the Study Area . Views of Sediment Classed as Type A Views of Sediment Classed as Type B . Views of Sediment Classed as Type C . Views of Sediment Classed as Type D . Views of Sediment ClassedcasaType E.. Generalized Map of the Surface Sediment Distribution in the Fort Pierce Grid Area Median Diameter of Sediments Comprising the Beach arid Shoreface in the Study Area. Location is indicated by latitude Sediment Characteristic of Beaches from the Study Area Sediment Characteristics of Beaches in the Study Area . Map of Potential Borrow Sites in Study Area.. Bethel Shoal is Judged to Contain Sediment Suitable for Beach Nourishment . 6 o Line Profiles Showing Acoustic Reflectors in the Bethel Shoal Area Isopachous Map of Sediment Thickness between the Water- Sediment Interface and the !'Z" Horizon underlying Bethel Shoal Isopachous Map of Sediment Thickness between the Water- Sediment Interface and the ''X' Horizon underlying Bethel Shoal Bottom aed and Survey Control in the Capron Shoal Area. 0 0 0 0.0 6 Line Profiles showing Horizons in the Capron Shoals Area Page 32 34 35 37 38 40 44 46 52 53 55 56 57 58 59 60 61 ILLUSTRATIONS (Continued) Figure Page 32 Isopachous Map of Sediment Thickness between the Water- Sediment Interface and the First underlying Acoustic Reflecting Surface in the Capron Shoal Area ......-. 62 33 Bottom Topography and Survey Control in the Central Part of the Indian River Shoal Area. This part of the Shoal contains sand suitable for beach nourishment ...... 63 34 Line Profiles Showing Horizons under the Control Part Of IndianwRaiversShOaleaiimm cucwuculle isin onue mNem icon kein ter MER mro esate 64 35 Sediment Thickness between Water-Sediment Interface and Blue Horizon in Central Part of Shoal COP ONT O 65 vi GEOMORPHOLOGY AND SEDIMENTS OF THE INNER CONTINENTAL SHELF PALM BEACH TO CAPE KENNEDY, FLORIDA by Edward P. Meisburger and David B. Duane Section I. INTRODUCTION 1. Background Ocean beaches and dunes constitute a vital buffer zone between the sea and coastal areas and provide at the same time much needed recreation areas for the public. The construction, improvement, and maintenance of beaches through the artificial placement (nourishment) of sand on the shore is one of several protection methods. This technique has gained prominence in coastal engineering largely as a result of the successful program initiated at Santa Barbara, California, in 1938 (Hall, 1952). Where the specified plan of improvement involves shore restoration and periodic nourishment, large volumes of sand fill may be involved. In recent years’it has become increasingly difficult to obtain suitable sand from lagoonal or inland sources in sufficient quantities and at an economi- cal cost for beach fill purposes. This is due in part to increased land value, diminution and depletion of previously used nearby sources, and added cost of transporting sand from areas increasingly remote. Material composing the bottom and subbottom of estuaries, lagoons, and bays, in many instances is too fine-grained and not suitable for long-term protection. While the loss of some fines is inevitable as the new beach sediment seeks equilibrium with its environment, it is possible to estimate the stability of the beach fill and therefore keep the loss to a minimum through selec- tion of the most suitable fill material (Krumbein and James, 1965). The problem of locating a suitable and economical sand supply led the Corps of Engineers to a search for new unexploited deposits of sand. The search focused offshore with the intent to explore and inventory de- posits suitable for future fill requirements, and subsequently to develop and refine techniques for transferring offshore sand to the beach. The exploration program is conducted through the U. S. Army Coastal Engineering Research Center (CERC). An initial phase in developing techniques for transferring offshore sand to the beach is described by Mauriello (1967). Formerly called the sand inventory program, it was begun in 1964 with a survey off the New Jersey Coast. Subsequent surveys included the in- shore waters off New England, New York, Florida, Maryland, and parts of ‘Delaware and Virginia. Recognizing the broader application of the informa- tion collected in the conduct of the research program toward the CERC mission, especially in terms of Continental Shelf structure (Meisburger and Duane, 1969), Continental Shelf sedimentation (Field, Meisburger and Duane, 1971), and its potential application to historical geology and engineering studies of the shelf, the sand inventory program is now re- ferred to as the Inner Continental Shelf Sediment and Structure Program (ICONS) . 2. Field and Laboratory Procedures The exploration phase of the ICONS program uses seismic reflection profiling supplemented by cores of the marine bottom. Additional support- ing data for the studies are obtained from USC&GS hydrographic boat sheets and related published literature. Planning, and seismic-reflection pro- filing, coring, positioning, and analysis of sediment obtained in the cores are detailed in Geomorphology and Sediment Characteristics of the Nearshore Continental Shelf, Mtamnt to Palm Beach, Florida (Duane and Meisburger, 1969). However, a brief description of techniques is germane to this paper and follows. a. Planning - Survey tracklines were laid out by the CERC Geology Branch staff in either of two line patterns: grid and reconnaissance lines. A grid pattern (line spacing about 1 statute mile) was used to cover areas where a more detailed development of bottom and subbottom con- ditions was desired. Reconnaissance lines are one or several continuous zigzag lines followed to explore areas between grids, and to provide a means of correlating sonic reflection horizons between grids. Reconnais- sance lines provide sufficient information to show the general morphologic and geologic aspect of the area covered, and to identify the best places for additional data collection. Selection of core sites was based on a continuing review of the seismic profiles as they became available during the survey. This proce- dure allowed core-site selection based on the best information available; it also permitted the contractor to complete coring in one area before moving his base to the next area. b. Seismic Reflection Profiling - Seismic reflection profiling is a.technique in wide use for delineating subbottom structures and bedding planes in sea floor sediments and rocks. Continuous reflections are obtained by generating repetitive high-energy, sound pulses near the water surface and recording "echoes" reflected from the bottom-water interface, and subbottom interfaces between acoustically dissimilar materials. In general, the compositional and physical properties which commonly differ- entiate sediments and rocks also produce acoustic contrasts. Thus, an acoustic profile is roughly comparable to a geologic cross section. Seismic-reflection surveys of marine areas are made by towing sound- generating sources and receiving instruments behind a survey vessel which follows predetermined survey tracklines. For continuous profiling, the sound source is fired at a rapid rate, and returning signals from bottom and subbottom interfaces are received by one or more hydrophones. Return- ing signals are amplified and fed to a recorder which graphically plots the two-way signal travel time. Assuming a constant velocity for sound in water and Shelf sediments, a vertical depth scale can be constructed to the chart paper. Horizontal location is obtained by frequent navi- gational fixes keyed to the chart record by an event marker, and by interpolation between fixes. A more detailed discussion of seismic profiling techniques can be found in a number of technical publications. (Miller et al., 1967; Ewing, 1963; Hersey, 1963; and Moore and Palmer, 1968). c. Coring Techniques - A pneumatic vibrating hammer-driven coring assembly was used for obtaining cores from the survey area. The appara- tus consists of a standard core barrel, liner, shoe and core catcher with the driver element fastened to the upper end of the barrel. These are enclosed in a self-supporting frame which allows the assembly to rest on the bottom during coring, thus permitting limited motion of the support vessel in response to waves. Power is supplied to the vibrator from a deck-mounted air compressor by means of a flexible hoseline. After the core is driven and returned, the liner containing the cored material is removed and capped. d. Processing - Seismic records are analyzed to establish the principal bedding or structural features in upper subbottom strata. After preliminary analysis, record data is reduced to detailed cross-sectional profiles showing all reflective interfaces within the subbottom. Selected reflectors are then mapped to provide areal continuity or reflective hori- zons considered significant because of their extent and relationship to the general structure and geology of the study area. If possible, the upper mapped reflector is correlated with core data to provide a measure of continuity between cores. Cores are visually inspected and logged aboard ship. After delivery to CERC, these cores are sampled by drilling through the liners and remov- ing samples of representative material. After preliminary analysis, a number of representative cores are split in order to determine details of the bedding. Cores are set up for splitting on a wooden trough. A circu- lar power saw mounted on a base which is designed to ride along the top of the trough is set so as to cut just through the liner. By making a cut in one direction and then reversing the saw base and making a second cut in the opposite direction, a 120-degree segment of the liner is cut. The sediment above the cut line is then removed with a spatula, and the core is logged, sampled and photographed. Samples from cores are examined under a binocular microscope, and described in terms of gross lithology, mineralogy, and the type and abundance of skeletal fragments of organisms. 3. Scope The area covered by this report extends along the east Florida coast and adjacent Continental Shelf, from Palm Beach (26°48'N) to the southern part of Canaveral Peninsula (28°27'N). The adjacent coastal segment, from Palm Beach to Miami, is covered in CERC's Technical Memorandum No. 29 (Duane and Meisburger, 1969). Figure 1 is a map of the location and major geographic features of the region. Field work in support of the study was accomplished between January and May 1965 by contract (Alpine Geophysical Associates, Inc.). Data collected and reported consists of continuous seismic reflection profiles covering 611 statute miles of survey line and 72 sediment cores ranging from 6 to 12 feet long (Figures 2 and 3). Basic data processing covered analysis and reduction of geophysical records, visual description and size analysis of sediment samples from the cores, and construction of large-scale navigation overlays showing the position of geophysical lines and cores. Field data was supplemented by literature pertaining to the region and by U. S. Coast and Geodetic Survey hydrographic smooth-sheet coverage at 1:40,000 scale. 4. Geologic Setting a. Hydrography - The shoreline of the study area extends 100 miles in a north-northwesterly direction from North Palm Beach (26°48'N) to near Canova Beach (28°08'N) thence northward and eastward 24 miles along the south flank of Canaveral Peninsula to Cape Kennedy (28°27'N). South from Palm Beach, the Florida shoreline has a north-south alignment. The study comprises coastal portions of the counties of Brevard, Indian River, St. Lucie, Martin, and Palm Beach, and includes the adjacent submerged plain of the Continental Shelf (Figure 1). The abrupt change in shoreline orientation near Palm Beach and the Canaveral Peninsula salient combined with changes in width of the Continental Shelf form geographic boundaries to the study area. Adjacent to the study area the Continental Shelf is complex. The major morphologic element of the Shelf is a submerged coastal plain with naturally divisible inner and outer zones and a well-developed shoreface zone. This shelf region varies from 2 to 38 miles in width and terminates at a break marking the top of the Florida-Hatteras Slope in water depths varying from 80 to 230 feet. The Florida-Hatteras Slope (name proposed by Uchupi, 1968) is defined as an incipient continental slope by Heezen, et al., (1959). It forms the western wall of the Straits of Florida in that part, of the study area lying south of 28°00'N. North of 28°00'N the slope descends to the Blake Plateau at about 2,300 feet (Figure 1). Within the study limits the immediate shore area consists of a low barrier island. North of St. Lucie Inlet, the barrier is backed by the broad lagoons of the Banana River and Indian River; south of the inlet, the barrier fronts a marshy swale traversed by the Atlantic Intracoastal Canaveral Bight Cocoa Beach ud Qa Indialantic oO \ ai) 28°00 ap) Ww 2 mm fraction of 46 representative sedi- ment samples. Important contributing organisms are listed in Table II, and some of the more common forms are shown in Figures 14 and 15. Identi- fication of biogenic constituents was based largely on Abbott (1954 and 1968); Morris (1951); Perry and Schwengel (1955); and Ryland (1967); nomenclature follows Abbott (1954). Dr. Joseph Rosewater and Mr. Walter J. Byas of the Mollusk Division, Smithsonian Institution verified the identification of a reference set of specimens. Most biogenic constitu- ents in the finer ( >2mm) fraction appear to be broken or smaller particles of the types of organisms identified. b. Fort Pierce Grid - Several sediment types can be recognized in the Fort Pierce grid area. Based largely on color and gross composition, sedi- ments in cores from the Fort Pierce grid are of five main types. In usual stratigraphic sequence these are: 1) Type A - clean, poorly sorted, brown, shelly sand; 2) Type B - gray, fairly well-sorted, calcareous sand; 3) Type C - silty gray sand and shelly gravel; 4) Type D - clean, light gray, fine to medium-grained, well-sorted calcareous sand; 5) Type E - white to light gray, generally poorly sorted, calcareous mud, sand, or gravel - often lithified. The relative stratigraphic position of these types is uniform through- out the study area. Such similarities point to a regional environmental uniformity during time of deposition of sediments of a given category. However, similar depositional conditions may have been recurrent or migra- tory, leaving deposits of similar material but unrelated in age. Likely 29 TABLE II CONSTITUENTS MOST COMMONLY FOUND IN COARSE FRACTION ( > 2im) FORT PIERCE SEDIMENTS MOLLUSCA Pelecypods Anadara transversa Say Anomalocardia cuneimeris Conrad Anomia simplex Orbigny Cardita floridana Conrad Chione intapurpurea Conrad Chione grus Holmes Corbula dietziana CC. B. Adams Crassinella lunulata Conrad Donax variabilis Say Glycymeris pectinata Gmelin Mulinia lateralis Say Nucula proxima Say Venericardia perplana Conrad Gastropods Crepidula fornicata Linne Olivella OTHER Barnacle plates and valves of the acorn barnacle. Algae-amorphous calcareous fragments of probable algal origin. Bryozoa - encrusting and small hermispheric lunulutiform types. Echinoids - spines and dermal plate fragments. 30 Chione grus (Holmes) Venericardia perplana Conrad Anadara transversa (Say) Corbula dietziana C.B.Adams 0 5 10 Millimeters Anomia simplex Orbigny Nucula proxima Say Mulinia lateralis Say Crassinella lunulata Conrad Figure 14, Exterior and Interior Views of Valves of Pelecypods Commonly Found in Whole or Eragmented Sediments from the Study Area. 3| Anomalocardia Chione intapurpurea Conrad lunulutiform Bryozoa acorn barnacle plates Figure 15. Views of Pelecypod and Skeletal Fragments of other Organisms which are Prominent Constituents of Sediment from the Study Area. 32 common factors creating similarity in sediment type are: 1) age of deposit; 2) sediment source; 3) environment and circumstances of de- position; and 4) post-depositional history. Interpolations of sediment distribution patterns between core sites have been based partly on the assumption that these apparent relationships are real. A small number of sediment samples from Fort Pierce grid cores do not fit into a classification. These sediments have been designated "U" (unclassified) in the core descriptions of Appendix C. Most of the un- classified sediments are either quartzose fine sands, found only in the shoreface area, or silty cohesive very fine sands which are more widely distributed (Wentworth classification is used throughout). All sediments within the Fort Pierce grid area having a brown colora- tion and devoid of silt or clay are classed as Type A (Figure 16). The group is variable in nature, but in most places is medium to very coarse, poorly sorted calcareous sand. Quartz is present in all samples, but the content ranges widely from a few percent to over 40 percent (Appendix B). The quartz grains are clear and colorless with a great variety of shapes. Large, well-rounded grains with frosted surfaces occur in many samples where they are mixed with the more common subangular to subrounded particles of quartz. Size analysis of insoluble residues from selected samples of Type A sediment are presented in Appendix B. Type A sediment contains the largest variety of organisms; most species listed in Table II are represented. Barnacle plates are very abundant, making up 50 to 70 percent of the identified fragments. Crassinella lunulata, Chione grus, Anomia simplex (usually fragmented) , Anadara transversa, and Crepidula fornicata are best represented. The skeletal fragments are mainly shades of brown, pink, white or gray with both rounded and freshly broken fragments mixed. Dark gray and brown well-worn shell fragments, with boring and solution holes, are scattered throughout, but not in large quantities. Foraminifers are rare. Nonskeletal carbonate material in the form of ooliths and pellets occur in Type A sediments, and locally in large quantities. Ooliths are especially common in samples from shoals near the seaward edge of the inner shelf. Although ubiquitous throughout the inner shelf area, Type A sediments have not been recognized in the few cores obtained from the outer shelf area (-70 to -230 feet MLW). Where found, Type A sediment is always upper- most in the colum. Over the flats, it usually occurs as a relatively thin blanket deposit less than 5 feet thick. Over shoals, it thickens appreci- ably, and seismic data indicates that some smaller shoals are entirely composed of this material. Type B sediment is a gray calcareous sand usually fairly well sorted, but may be silty or poorly sorted in some places (Figure 17). This mate- rial underlies Type A sediment where found. The position, size similarity, and composition of Type B material suggests that it is a facies of Type A 33 m », 2 « we i al a) A pat Core 67A -3 Feet Core 76 -1.0 Feet (0) 5 10 eee ieee res Millimeters Figure 16. Views of Sediment Classed as Type A. Note differences within the class. Core 87 Top 34 2 ‘d © ; we Core 73B - 5 Feet O 5 10 eee ee ica | Millimeters cman j Figure 17.. Views of Sediment Riga Classed as Type B. Note greater Core 41 — 7 Feet uniformity within the class. ~ 35 sediment. The chief difference between Types A and B is the color of Type B constituent particles which range from white through gray to black (contrasted to the predominant reddish and brown colors of Type A material). Some finer samples of Type B material resemble the fine, well-sorted, carbonate sand described below as Type D, and a relationship may exist. In many places, however, where both types B and D occur in the same core, they are separated by a silty, sandy shell gravel (Type C) and the B‘sedi- ment is darker in color, less well sorted and richer in barnacle plates than the D material. Type C sediment is characteristically gray, silty, very coarse skeletal sand to sandy shell gravel (Figure 18). Usually, it is slightly cohesive when wet, and dries to friable lumps of silt, sand and shells. Quartz particles, present in small quantity, range from silt-size to very coarse, irregular, but well rounded grains. Size analysis of insoluble residues from typical Type C sediment are contained in Appendix B. Biogenic remains in Type C sediment show close similarity to the Type A assemblage. Anadara transversa, Anomia Simplex, Chione grus, Crassinella lunulata, and Crepidula fornicata common in Type A sediment, are also well represented in Type C. Barnacle plates are abundant (25 to 50 percent) but less so than in Type A. Venericardia perplana and fragments of Chione intapurpurea appear to be more common than in other sediment types. The condition of shell fragments varies from relatively "fresh" to gray or black well-worn pieces, often pitted by sponge and algal borings. Dark colors predominate. Nonskeletal carbonate material consists mostly of sparse pelletoid and oolitic-shaped grains which occur in some cores. Type C sediments are common throughout the inner-shelf area, but are rarely exposed at the surface. Type D sediment is light gray or pale brownish gray, fine-to-mediun, well sorted calcareous sand (Figure 19). Locally, it contains shells and shell fragments in sufficient quantity to constitute a second size mode, but most often the sediment has few large inclusions. Constituent par- ticles are generally rounded and sometimes polished. White, gray or black colors predominate, and the contrasting light and dark colors often impart a "salt and pepper'' aspect to this sediment. Most Type D particles are calcareous and of probable organic origin, although few are identifiable except for small foraminifers. These foraminifers are relatively abundant in the finer fraction, and are of diagnostic value since small species rarely occur in other sediment types of the study area. Crepidula fornicata is probably the most common mollusk overall in Type D sediment; however, at least locally, Mulinia lateralis is most abundant. Venericardia perplana and a small species of Olivella are also common. Crassinella lunulata an ubiquitous species in all other sediment 36 Pier EN Core 42 - 2 Feet Core 78 -I.0 Feet (@) 5 10 Uist | pene ee] Millimeters Figure 18. Views of Sediment Core 40 -5 Feet Classed as Type C. 37 e.' 3 . : of} Py ee tf ayeedo, Ms ne Pe & * e . ta) -5 Feet Core 77 -7 Feet Core 36 10 Millimeters Views of Sediment Classed as Type D. an q oO u =) lef) dd oa 38 types of the area is rare in Type D sands, as are barnacle plates which occur in quantity in Types A, B, and C sediment. Type E material is characterized by its white or very light gray color. This material is highly variable in size and in its degree of lithification (Figure 20). In typical cores, layers of lithified and semi- lithified material are interspersed with sediment layers. Many of the unlithified layers contain granules and pebbles of calcarenite probably weathered or redeposited from the lithified layers. The size range of Type E material varies from silty calcareous clay to coarse calcareous sand, shell gravel and pebbles. Most of the sand- size material is biogenic. Fragmentation of the skeletal sand-size material is usually well advanced and identifiable fragments are sparse. Indurated Type E rocks appear in cores in the form of layers or discrete pebbles and angular fragments mixed with unconsolidated sedi- ments, generally similar to that comprising the indurated material. Indurated fragments obtained from cores on the outer shelf consist of white medium-grained calcarenite containing shell fragments, foraminifers, quartz, and many oolitic or pelletoid grains. Individual grains are frequently well worn, and many are polished. Cementation occurs only at points of grain contact, and there is little if any infilling of interstices. Type E material occurring in cores of the inner shelf is more variable. In places it consists of white calcareous silty or sandy clay which dries to a very hard rocklike substance. Other E sediments and indurated material from the inner shelf generally are light gray or tan, and the indurated material is finer grained, denser and more compact than that from the outer shelf area. Redeposition of calcium carbonate in interstices appears to have accounted for greater density although grain size and sorting may be equally important. It is difficult in most cases to determine if indurated fragments in Type E material are the result of the coring tube penetrating lithified layers or if the fragments are redeposited from a higher source. Ina few cases, a solid plug of rock in the core is evidence of penetration of an indurated layer. Angular ''fresh'' appearing fragments also evidence the breaking up of a layer by penetration of the corer. Occasional rounded pebbles of calcarenite are probably redeposited. Type E sediments are most variable in terms of coarse constituents. Fragments of calcarenite, rare in other types, are common. Mulinia lateralis and Glycymeris pectinata are the most common pelecypods. Crepidula fornicata is common, as are fragments of other species of gastropods. Barnacle plates are absent in some samples and abundant in others. Skeletal fragments are for the most part white - or near white - often worn and occasionally partly embedded in calcareous material. 39 eg > ae ig ~ ry Ba Y “Dene Core 44 -5 Feet Core 42 -8 Feet O 5 10 EY mar smer etary eerie cee | Millimeters ! : Figure 20. Views of Sediment yt 5 Classed as Type E. Views are Ee: 2 Ne oy of unconsolidated "facies". rr ares CREE Type also occurs as lithified Core 90 -9Feet "facies" within the study area. 40 Type E material is the most widely distributed of all sediment types in the Fort Pierce grid area. It occurs at the surface in many places, usually on the outer shelf. The pattern of occurrence and its association with the blue reflector strongly SUBEOSES that this material continuously underlies the entire grid area. Among the unclassified sediments a number contain quartzose sand. These samples are all from shoreface cores, and possibly represent mate- rial winnowed from the quartzose deposits of the present beach. Shells of mollusks, particularly Crepidula fornicata and Mulinia lateralis, are mixed with the sand matrix, but the sand fraction itself contains little carbonate material. This sediment is designated UI in Appendix C. Most of the remaining unclassified samples are silty, cohesive, very fine sands which do not appear to be restricted to any particular area or stratigraphic position. They are possibly localized deposits of fine material winnowed from overlying or adjacent units and are designated U2 in Appendix C. c. Reconnaissance Areas - Almost all cores taken on the Fort Pierce- Cocoa Beach reconnaissance lines contain gray, silty, clayey material in the upper layers. Varying amounts of shell are mixed with the silt-clay matrix; generally shell increases in size and density with depth. In some respects this material resembles Type D material. In most places, it is underlain by a light tan to white calcareous clayey unit containing many broken shell fragments, some of which are chalky and very friable. When dry, this material is extremely hard. No material closely resembling Fort Pierce type sediments is contained in these cores from the reconnaissance area. It is thought significant that the disappearance of Type A material coincides with the disappearance of shoals in the inshore area, and (with the exception of Thomas Shoal) from the offshore area. The relationship of this sediment type and surface topography appears to be close. Cores north of about 28°10'N (Canaveral Bight) indicate that the Bight area is blanketed with a deep deposit of relatively uniform clayey silt containing few shells. This deposit probably forms the shallow inner level of the 50-foot flat in Canaveral Bight. The fineness of the mate- rial suggests it has been deposited in a low energy environment created by Canaveral Peninsula and its off-lying shoals. Core 181, which penetrated material differing from that found in other cores of the reconnaissance area, contains the only sand potentially usable for beach fill. A layer of quartzose, medium-to-coarse sand with varying amounts of shell fragments in the upper and lower parts of the core appears to be suitable for fill. A thin layer of clayey sand con- taining woody material overlies the first quartzose layer. The extent, form and orientation of this deposit cannot be determined from available data. It is, however, a promising place for further investigation, should offshore sand supplies be needed in the general vicinity. The lower part 4| of a nearby core, Core 182, also contains somewhat anomalous material in the form of a shell gravel consisting almost entirely of well preserved shells of Mulinia lateralis, some shells of Donax variabilis and quartz. Whether this stratum is a facies of the material found in the adjacent Core 181 is not known. Very little data is available on sediments in the reconnaissance area southward from Fort Pierce grid to Palm Beach. Only two cores were taken in this area - both near the southern border of the grid. Moe (1963) reports a rolling sand and shell bottom in the area with coral rock reefs at 30, 70, and 130 to 140 feet; the shallow reef is obscured by sedimentation in many places. Material found blanketing the shelf at Palm Beach and southward to Boca Raton consists of a fine, well sorted, gray quartzose sand dissimilar to any sediment found in Fort Pierce grid except perhaps Type D. A transitional zone between the typical Type A surface sediment of Fort Pierce grid and the gray sand body at Miami Beach must occur in the reconnaissance area. If the presence of Type A sediment is indicated by shoals (as seems to be the case), this sediment type probably persists as far south as 27°05'N because shoals similar in form to those found in the Fort Pierce grid occur here. 42 Section IV. INTERPRETATION 1. Sediment Distribution and Origin a. Fort Pierce Grid Area (1) Bedding Sequence and Extent - The usual vertical sequence of cored sediment layers in Fort Pierce grid from the lowest is, E, D, C, B, and A. The stratum containing Type E material is believed to be continuous throughout; other sediment types recognized are not everywhere present and it appears from seismic and core data that none extend far seaward of the inner shelf (Figure 21). Type E material is found in 23 of the 62 cores from the grid area, and in these it persists to the bottom of the core. In the remaining 39 cores - particularly those of the inner shelf shoals - overburden thickness prevents core penetration to Type E level. Cores and geophysical profiles from the outer shelf and descrip- tive data from the study by Moe (1963) indicate that extensive exposures of Type E material may occur in that zone. A large area of exposure or near exposure on the inner shelf is centered about 5 miles east of Fort Pierce Inlet (Figure 21). Elsewhere on the inner shelf, local exposures may occur in swales between shoal areas. Type D sediment occurs in 17 cores from the grid area. Where re- covered, Type D sediments are either the bottom layer in the core or overlie Type E material. The close resemblance of sediments in many samples of Type D with underlying E material, suggests that it may be derived partly from reworking of this underlying stratum. Type C sediment is second only to Type A in frequency of occurrence in the Fort Pierce grid cores. It is probably nearly continuous through- out the inner shelf area. Only Types A and B, and occasional miscellan- eous unclassified sediments, overlie the C layer. Surface exposures of the material are uncommon. Type A sediment is the characteristic surface sediment of the inner shelf area. Nearly all inner-shelf cores contain A sediment as the sur- face layer. Usually Type A sediment overlies Types B or C, but it is also found in direct contact with Types D and E. Thickness of the sediment layers revealed by Fort Pierce cores is variable. Type A sediments vary from a foot to at least. 12 feet in depth and possibly reach more than 30 feet’in places. The thickness of the Type A layer is generally related to shelf topography, being thick under shoals and thin in the flats and swales. Sediment Types B, C, and D are relatively thin bedded - average sections are about 5 feet or less. The E layer has not been completely penetrated by cores, thus there is no direct evidence of thickness. Available data indicate a thickness of over 10 feet. Most of the sediments which were not classifiable consisted of silty, cohesive, fine sands and probable mixtures of sediment types 43 \ \ @65 \ \ \ 034 1064 SURFA DISTRIBUTION EXPLANATION @ Core YY, Quartz > 25% [J quortz < 25% Exposed == H } <5 Ft. Overburden too e=_. Unconsolidated ==" Semiconsolidated ae Scole in Yords 2 s_s_o 8 ——s 2000 1000 0 2000 4000 Figure 21. Generalized Map of the Surfate Sediment Distribution in the Fort Pierce Grid Area. 44 classified above. Type Ul sediment is found in a few cores, but only from the shoreface area. The high quartzose content suggests this ma- terial may be largely derived from quartz-rich deposits on the present beach. The source of most sediment particles found in Fort Pierce grid cores is the benthic biota. Organisms contributing to the material - insofar as can be determined - are indigenous to the area. Quartz, the only noncarbonate element present in significant quantity, must have’ been derived from the Piedmont Province since no primary quartz-bearing rocks crop out on the Florida Peninsula (Puri and Vernon, 1964 and Pilkey, et al. (1969). Net drift of sediment on the east Florida coast is south- ward (Watts, 1953; Giles and Pilkey, 1965; Bruun, Geritsen and Morgan, 1958). Studies of the southern Atlantic Shelf indicate that shelf sedi- ment transport parallel to shore may not be an important process (Pilkey, 1968 and 1969). Thus, movement, if any, is probably in a general onshore- offshore direction. The dominant carbonate suite may have been created in recent times by organisms inhabiting the area of accumulation or may have originated outside the grid area and subsequently entered as detrital sediments. A third possibility is that the skeletal fragments were reworked from older underlying formations. Available information indicates all three processes probably played a part in sedimentation of the inner shelf area, and through time the dominant depositional process may have differed for different sediment types. The deepest, and presumably oldest, stratum reached by Fort Pierce cores is the stratum containing Type E material. The top of this stratum is tentatively correlated with the blue acoustic reflector (Figures 7, 8, and 9). It is believed that the E stratum was deposited during or prior to the late Wisconsin regression commencing some 30,000 years Before Present. One evidence of this minimum age is that indurated layers occur within the Type E stratum. Induration of clastic carbonate sediments strongly - but not conclusively - indicates exposure to subaerial or littoral conditions (Ginsburg, 1957; Friedman, 1964), therefore suggesting exposure during the late Wisconsin regression or earlier. A further in- dication is that projected depths of the blue reflector under the coastal ridge are equal to or below the top of the Anastasia formation in the coastal region; Anastasia rocks are presumably Sangamonian (last interglacial) and possibly earlier in age (Cooke, 1945; Puri and Vernon, 1964). Type E material from the outer shelf does not resemble descriptions given to Anastasia rocks in the coastal area. However, the Anastasia is lithologically variable and little is known concerning its character - or existence - seaward of the coastline. Two cores from the inner shelf area, 45A and 34, contained plugs of rock in the cutter head which resemble rocks presumed Anastasia found near the shore at Fort Pierce. Elsewhere the Type E material of the inner shelf is not inconsistent with the wide- ranging lithologic description of the Anastasia Formation in coastal Florida. 45 *SsoTpnys [OI}ZUOD UOTSOZO Yyoeeq LooUTSUq Jo sdzoj poysttqnd worz pautezqo uotzyewxXoJUT ‘N,OS$,LZ 02 NiST,LZ woLz eIep TOF ydeodxg ‘apnzTyeT Aq peeoTpUT ST uoTzeD0T ‘every Apnis 94} UT adeFoLOYS pue yoeeg oy Sutstidwoy sjuswtpas Fo IojoweTq ueTpeW “ZZ oAN3TY BPNjyO7 YJJON fA RUN tr AEA IN EU A A ALUN LOM AUC AT USEPA Us LU A je LA URL Le Ue aE) 0 a w oO o2+ OniK JaJQWDIG UDIPa Iu a21S Buisoasou| o2- j294g|— —--—-—- — 12049 - a40yse04 oEe- Ob- @10US90 Gea NOILVNV 1dX3 oG- 46 Unconsolidated sediments lying aboye the blue reflector may have originated largely outside the area of deposition or have been largely derived from local sources. Since no streams discharge directly on the Florida coast south of Jacksonville Beach, this common source of terrig- enous sediment is not considered active here. Pleistocene drainage may have played some part as a previous source, but no evidence of important contributions from this source is available. A possible source of sediment from outside the grid area is littoral drift alongshore coupled with offshore transport to the shelf area. Exist- ing beach sediments north of Cape Kennedy are considerably finer and more quartzose than those of the study area, thus could be contributing only minor amounts of material presently on the beach and shelf in the Fort Pierce grid. Net littoral transport in southeast Florida is southward (Watts, 1953); thus, drift from the south is also an improbable source of beach sand near Fort Pierce. The most likely sources of beach sand are coastline erosion and local shell production. Shelly quartzose sand similar to that of the beaches is available in preserved Pamlico Age sands of the-coastal upland. Storm wave erosion of this source could play a significant role in littoral sedimentation. Shell production is high, especially in the vicinity of the inlets. Additional shell and quartz debris is probably derived locally from erosion of coquina outcrops reported in the shallow waters close inshore (USCE, 1967 and 1968); although some of these outcrops may in fact be sabellariid reefs (Kirtley and Tanner, 1968). Some cores from the shoreface area contain quartzose sand similar to the beach sands. Elsewhere on the shelf, good evidence of beach-derived sand is lacking. The coarser texture of shelf surface sediment compared to the beach, and progressive diminution of sand size transported from shore into the sublittoral shoreface as evidenced by the size data of Figure 22, tends to indicate that large quantities of littoral sand are not reaching the shelf proper at the present time. In addition, the rounded and polished character of shell fragments in beach sand, though present in shelf surficial sediments, is not characteristic. Difference in quartz-carbonate ratios between the beach and offshore surficial sedi- ments is substantial. If sand does reach the shelf from onshore deposits, it is greatly diluted by carbonate material derived from other sources. If the sediment were derived from outside the area, the most probable sources are the adjacent shelf areas to north and south. Characteristics of the shelf to the south of the Fort Pierce grid to north of Palm Beach are not well known, but south of Palm Beach, reliable information is available. Between Miami and Boca Raton (24°45'N to 26°20'N) the near- shore shelf contains white to gray calcareous sand alternating with rocky ridges and flats (Duane and Meisburger, 1969). Examination of repre- sentative samples from this shelf shows that the major constituents are Halimeda segments and mollusk shells. Halimeda and other common constituents such as alcyonarian sclerites and large peneroplid foraminifers are missing in Fort Pierce grid samples. 47 Barnacle plates, one of the most common constituents of Fort Pierce grid cores, are uncommon in the Miami-Boca Raton shelf sediments. It is in- teresting to note that De Palma (1969) found large quantities of barnacles on test panels off Fort Lauderdale. Their scarcity in CERC sediment samples from the Palm Beach-Miami area may be a result of the inability of the barnacles to successfully compete with other organisms living on the natural substrata. North of Boca Raton, the inner part of the shelf is covered by a blanket of homogeneous fine gray quartzose sand. The outer part of the shelf has not been sampled by cores, but is believed to contain material similar to shelf sediments south of Boca Raton. Except for some similarity of Type D sediment at Fort Pierce grid to the well sorted gray sands between Palm Beach and Boca Raton, there is no evidence in sediment constituents of significant interchange between these regions. The similarity between Type D sand and the southern gray sands is largely in coloration and sorting. The chief dissimilarity is in the larger grain size of the material at Fort Pierce and the higher quartz content of the sand found south of Palm Beach. While the gray sand occurring off Palm Beach could be the product of southward transport- ation of Type D material (with concomitant downdrift reduction in size and carbonate content), it does not seem possible that the gray sands off Palm Beach could have been the source of Type D material. Another possible source of sediment for Fort Pierce grid is on the shelf to the north. Cores from Cape Kennedy are now under study for a forthcoming ICONS report, but only preliminary analysis is available. These analyses show that sand similar to that found at Fort Pierce is present at Cape Kennedy; however, much dissimilar material is also present. On the whole, Cape Kennedy sediments are more quartzose than those at Fort Pierce and cores from the Fort Pierce-Cape Kennedy reconnaissance lines do not contain material which obviously indicates transfer of sediments within the depth range sampled (40 to 55 feet). If material is being brought down presently from the Cape Kennedy shelf to Fort Pierce grid it must be transported outside the area covered by. cores. It is significant that the shelf between Cape Kennedy and Fort Pierce is slightly deeper and generally free of the topograhic irregular- ities which would be expected if shoals were migrating southward from the Cape Kennedy area (Figure 5). Also if any large quantities of sand were moving, either in waves or by sheet flow, southward from Cape Kennedy, one would expect that infilling of the deeper embayed section of the shelf off Canaveral Bight by sandy sediment would occur before much material was transported further southward. Fine sediments (silt.and clay) ponded in Canaveral Bight are evidence that sand is not now being bypassed through this area either from north or south. Material may have been exchanged between the Cape Kennedy and Fort Pierce areas at a past time of lowered sea level, but firm evidence of continuity or direct relationship requires additional sediment samples 48 and more detailed analysis of constituents. Poorly sorted sediments such as Type C could not have been transported as entities from one locale to the other since the transportation processes would have better sorted the material. The similarities between some sediments in the two areas can be attributed as well to common factors in the depositional environment and history as to actual interchange of material. The foregoing discussion leads to a conclusion that most particles in the shelf sediments of Fort Pierce grid are locally produced and - at least at present - only relatively small quantities of sediments are entering the grid from adjacent shelf areas or from the littoral stream. (3) Rate of Accumulation - If the surface of the stratum con- taining Type E material is indeed pre-Holocene, the overlying sediments represent accumulation during, and subsequent to, passage of the Holocene sea across the shelf platform. Since nearly all non-Type E sediments lie on the inner shelf, deposition in this zone would have commenced when relative sea level rose above -70 feet MLW. Assuming that this region has been structurally stable during the period in question, the onset of transgression across the inner shelf would have occurred at about 8,200 years Before Present according to data from Curray (1964) and about 7,200 years Before Present based on the sea level curves of Milliman and Emery (1968). Both curves indicate a rate of rise which would have brought the sea landward across most of the inner shelf (to -40 feet MLW where the slope changes from 1 on 1,300 to 1 on 80) about 1,000 years after the onset. Using an average sediment thickness above the blue reflector esti- mated from the isopach map of Figure 8 to be about 7 feet and a sedimenta- tion time of about 7,000 years, the average rate of accumulation is only about 1 foot in 1,000 years. It seems unlikely that sedimentation of the inner shelf has pro- gressed at a steady rate during this period. Increasing depth over the shelf during the last transgression and ancillary variations of conditions affecting local shell production probably also affected accretion rates so that periods of relative increase or decrease in rate of accumulation are likely to have occurred continuously. 2. Sand Requirements In a 1965 appraisal of Florida beach conditions (USCE, 1965), the Jacksonville District, Corps of Engineers, listed about 50 percent of the shoreline within the limits of this study as subject to severe erosion. The beach was found to be generally narrow and low, and dune heights rarely exceed +15 feet. Beach Erosion Control studies have been completed for only two of the four counties in the study area: Brevard County (USCE, 1967) and Martin County (USCE, 1968). Sand requirements for beach mourishment summarized earlier (Duane, 1968) are in Table III. The total sand requirements for Martin County and that part of Brevard County south of Canaveral Harbor 49 TABLE III FILL REQUIREMENTS FOR MARTIN COUNTY, AND BREVARD COUNTY SOUTH OF CANAVERAL HARBOR INLET Initial Annual 50-year Martin County Area Fill* Nourishment Nourishment* Jupiter Island 2.43 15 7.5 Jensen Beach 5 OO .024 1.2 Stuart Beach 5 aly 024 ho Total 2.82 198 9.9 Total initial and nourishment fill in 50 years Wo 72 Brevard County (south of Canaveral Harbor Inlet) City of Cape Canaveral 988 . 240 12.00** Patrick AFB .70 . 082 4.1 Indialantic and Melbourne Beaches . 603 068 3.4 Total 2.291 . 390 19.5 Total initial and nourishment fill in 50 years of which 12,000,000 would be furnished by sand transfer 21.79 * x10° Cubic yards ** To be furnished by sand transfér plant at Canaveral Harbor 50 Inlet amounts to 34.5 million cubic yards for initial restoration and 50 years of nourishment. Of this total, about 12 million cubic yards may be furnished by sand bypassing at Canaveral Harbor (USCE, 1967); the remainder must come from borrow sources. Figure 22 shows the median diameter of sand on the beaches and in the nearshore area. Figures 23 and 24 show typical beach material from the study area. In general, the data indicate that desirable borrow material for projects in the area should have a median diameter in the range 0.3 to 0.5 mm (1.74 to 1.0 phi) and contain the same size classes as the original beach material. 3. Suitability Sand from beaches bordering the study area is not closely similar to any sediment found in the offshore surface or subsurface deposits (Appendix B). Type A sediment is the closest in character to the beach deposits, but significant differences between the two exist. Generally, the beach sands are better sorted and more quartzose than those found offshore in the study area. Quartz content of several midtide samples from the area is around 65 percent compared to 20 to 30 percent or less in offshore surficial sediments. Shell fragments which are important, but not dominant, constituents of the beach sediment are mostly finely broken, well rounded and polished. Beach drift shells collected near Fort Pierce Inlet contained many thick-walled pelecypods such as Arca zebra, Noetia ponderosa and Glycymeris. Such species are probably well repre- sented in the shell fraction of beach sands since the thick walls provide Sizeable grains resistant to fine fragmentation. Thin walled shells readily break down into fine fragments under the vigorous regimen of the littoral environment. Because the offshore potential borrow sands contain significantly more shell material than the adjacent beaches, it is important to know if this material is likely to break up into fine fragments under wave attack on the beach face. For Type A sediment - and this is the only well-suited fill material - the probability is that most of the shell fraction will withstand wave attack on the beach as well as do the shell fragments in the existing beach material. The major shell constituent of Type A sedi- ment is the barnacle plate which appears to be resistant to mechanical degradation, especially in comparison to algal material such as Halimeda found in abundance in the Miami area. Species of Arca, and large speciments of Crepidula should also pro- vide suitable sand fragments, while more friable materials such as the shells of Anomia simplex, may be soon lost from the sand fraction. It is estimated that on the whole, Type A sediment should not initially lose more than a small fraction of its sand-size material due to abrasion, and that the remaining material will not degrade at a greater rate than the existing beach sand. 5| Beach Sample Ol2-78 5 10 [i PES aes a | Millimeters An a ; pot Figure 23. Sediment Characteristic of Beaches from the Study Area. Beach Sample ON 2=7% | Locations are shown on Figure 25. 52 -62 Beach Sample Ol2 Beach Sample Ol2-64 fe) Millimeters Sediment Characteristics of Beaches from the Study Area. Locations are shown on Figure 25. Figure 24. 38) Beach Sample Ol2-60 The size of quartz particles in beach sands and those found in selected offshore sediments are within the same size range (Appendix B). In fact, the quartz fraction (insoluble residue) alone of Type A sediments on Bethel Shoal has a median (and mean) diameter equal to or coarser than the beach sands. 4. Potential Borrow Areas Three of the 12 shoal areas within the Fort Pierce grid are judged to contain the best material for restoration and nourishment of beaches (Figure 25). Two of these: Capron Shoal and the middle section of Indian River Shoal lie close inshore; the third, Bethel Shoal, is located well offshore. Bottom topography, isopach maps and selected profiles for each of these three sites are presented in Figures 26 through 35. Bethel Shoal contains an estimated volume of 175 x 10° cubic yards of unconsolidated material above the blue horizon (Figure 26). Good Type A material was obtained in cores 69 and 71 on the upper part of the shoal to a minimum depth of 10 feet. The lateral extent and total depth of this better material is not accurately known because of limited core data. Estimates based on an assumption that the base of the better material is either at the first or second continuous subbottom reflector within the shoal proper (reflectors x and z, Figure 27) give volumes of 16.5 x 10 cubic yards and 55.2 x 10© cubic yards respectively (Figures 28 and 29). On the basis of existing data, it seems most probable that the volume above the first reflector is the best estimate and that below this reflector the material is considerably finer in texture. Capron Shoal, centered about 4 1/2 miles southwest of Fort Pierce Inlet and 3 miles offshore, contains an estimated volume of 112 x 106 cubic yards of sediment above the blue reflector (Figures 30 and 31). Cores 32 and 53, taken near the crest of Capron Shoal, contain about 7 feet of Type A sediment. Underlying the Type A layer is a Type D strata of poorer quality. The base of usable material is believed to correlate with a reflector in the shoal proper (first subbottom reflector) in Figure 31. Volume above this reflector is 65.4 x 106 cubic yards (Figure 32). Core 38 in the middle section of Indian River Shoal contains suitable material to the bottom of the core (10 feet long) (Figure 33): It is believed that the material rests directly on the blue reflector (Figure 34). Assuming that it does extend to the blue reflector, the volume of usable sand in middle Indian River Shoal is 10.3 x 10° cubic yards (Figure 35). Elsewhere, Indian River Shoal may contain comparable material; cores 41 and 43 on the shoal section south of the middle contain fair material (Type A). In addition to the three possible borrow sites above, other shoal areas in the Fort Pierce grid, all containing Type A sediment, may be Text resumed on page 66 54 80°45! 30° 15° 80°00' 79°45! + + + “Fo 28°30" Eau Gallie 012-37 012-76 Melbourne zero} 012-75 ol2- #Q e 39) Thomas Shoal 012-73 b> + + Ww - V4 012-70 Bethe! Shoal Vero Bedell 69 Vy River Shoal 712-31) 012-67 “af ‘ hi a _ 012-65 Y A Shoal Fort Pierce Ol2- ox 712-7 712-8 538 Sy 712-10 \4 012-59 Lae -|. POTENTIAL BORROW AREAS = |) EXPLANATION S¢ Lucie River we Best Foir Questionable eoi2-58 Beach Samples peas Shoal St Lucie Shoal \7 a Statute Miles == 5 0) 5 10 15 ig oot a 012-53 a. 80°45" 30° 15° 80°00 eel es ney dee | Figure 25. Map of Potential Borrow Sites in Study Area. Note locations of beach samples illustrated in Figures 23 and 24. 55 eo nO BOTTOM TOPOGRAPHY ,,. EXPLANATION @® Core Survey Line and Navigation Fix 2515 Scale in Yards 0) 500 Figure 26. Bethel Shoal is Judged to Contain Sediment Suitable for Beach Nourishment. 56 uwnjoy juawipas ul (44) yydaq uwnjo juawipas ul (4j) yidaq IOJ eep ITTJowoT[Nuesy9 UOZIOH MO}|aA =A UOZIUOH anjg=g X14 UOIJDBIADN = bGE] NOILVNV 1dX4 D9 |DJUOZIIOH ON WOHS TSHLA9 ‘gq xtpuoddy ut ore sero. UT sjUSWTpas “SOUT[TYOCI} JO UOTIEIOT IOF 9Z 9aINSTy 9ag ‘eazy [TBOUS [EeYI9q OY. UT SLOJDOT Joy BTASNody BuTMOYS SOTTFOLg SUT y] "LZ emnsT A (panuijuod) 11 SN = =f Z |2 9409 @ 76 8b6l 6b6l Osé6! 1 3N ° oS da Océ! IG6l £S6l bS6l 9S61 WEN) > HH} p- 0622 6822 2822 982e Sele pele ooooaooso unTOOON 8282 6282 o¢8e c£82 ee8e VOL repel Aes Ol 3409 Se == % a 69 9109- | gle! Gel bel TT aur 12Z¢1 Ole! 69¢1 uuinjon 940M Ul (45)-UF day UWNI|OD Ja;OAK Ul (44) 4b 57 BETHEL SHOAL ISOPACHOUS MAP SURFACE TO Z HORIZON EXPLANATION ©. Core : Novi Fi ao Survey Line and Navigation Fix mrOR Scale in Yards 500 250 0 500 Figure 28. Isopachous Map of Sediment Thickness between the Water- Sediment Interface and the ''Z" Horizon Underlying Bethel Shoal. 58 BETHEL SHOAL ISOPACHOUS MAP SURFACE TO X HORIZON EXPLANATION © Core 27°38" ia Survey Line and Navigation Fix 2515 Scale in Yards 500 250 0 500 Figure 29. Isopachous Map of Sediment Thickness between the Water- Sediment Interface and the "X" Horizon Underlying Bethel Shoal. 59 2] Gea, 800), ; 26! Shoreline 2g! EXPLANATION ® Core Survey Line and Navigation Fix /6' 280 S225, v 800 22! Figure 30. Area. CAPRON SHOAL BOTTOM TOPOGRAPHY > oO BY Ge wt SS S x S Cy APPROXIMATE SCALE IN FEET 3000 1500 O 3000 wv ~ bottom Topography and Survey Control in the Capron Shoal Capron Shoal contains sand considered suitable for beach nourishment. 60 Depth (ft.) in Water Column = EAST 59 60 6 62 63 OF 0 20F 20 40 —y= Ss ————= == : oe * Gy Y Y = > —s 80 8 100 100 = LINE 0 & > wn 02864 2865 2866 2867 2868 2869S 20F ay = aoe L == ee = 7 8 8 60 60 E = Y. Y | Y i 80 100 100 LINE P 6 2892 2893 2894 2895 2896 c 5 20F sj20 E S| 40E {40 aa eo oF Feo = 100 1089 1087 1085 D iS) PUT TTT Depth (ft.) in Water Column is i=} LINE S 2939 2937 2936 2935 ons 2). Loboitititit SS) LINE T B = Blue Horizon EXPLANATION 1088 = Navigation Fix Y = Yellow Horizon CAPRON SHOAL No Horizontal Scale Depth (ft.) in Sediment Column 100 Figure 31, Line Profiles showing Horizons in the Capron Shoal Area. 6l Boag, 18 iN N \ \ BY > ~ 12" & ° & / I) i # / ! i ~ | A Ir 29" lo IN l= iS Jo °o a [2 3 < 1S L | 2 f= n LE e2e [= | | ! I ~ Limit I 2g! L | <6" | | I l I \ | \ T.! 32 EXPLANATION” \ \ ® Core © ie Survey Line and Navigation Fix = h APPROXIMATE SCALE IN FEET CAPRON SHOAL eae “B05, 3000 1500 0 3000 6000 ISOPACHOUS MAP £9 SURFACE TO FIRST REFLECTOR Vv ° ° ~ me R | S @ eee Figure 32. Sediment Interface and the First Underlying Acoustic Reflecting Surface in the Capron Shoal Area. 62 $000, Isopachous Map of Sediment Thickness between the Water- ¥ OO \ INDIAN RIVER SHOAL — BOTTOM TOPOGRAPHY — 27°36 EXPLANATION © Core ( Survey Line and Navigation Fix 1322 ; Scale in Yards 500 250 O Figure 33. Bottom Topography and Survey Control in the Central Part of the Indian River Shoal Area. This part of the Shoal contains sand suitable for beach nourishment. 63 “‘quoutpas Fo sasXkTeue 2T1.OWoOTNUeII oF q xtpueddy pue sautTyoe1, Jo uoTed0T OF ¢¢ aANBIy veg ‘TeoYS TOATY UeTpuy FO Leg TOLJUOD) 9Y} LIOpunN SUOZTIOH BUTMOYS SETTJOIg SUTT “ps OANBTY [DIS |DJUOZIJOH} ON UOZIJOH MO}|AA = A UOZIJOH anig =g TVOHS Y3SAIY NVIGNI xia) ue! DBIADN|={OGSe NOILVNV 1dx4 € 3NI7 |, 001 08 08 09 A is * k 09 oO is] S op g 8 g oF = 02 _ © 5 ° Biel a au 6I¢ Oee! eel 22¢ e2e! ois wn =) o = 5 aan 8 $ 001 = S 08 F pe = 3 09 A o9 3 oF = a ee ———— ov oe BE 2109 2 i) LbGe £ ay] 8bSe 6bS2 oss2 Igce 2SSe 27°39! -+- 3 oo +. 27°39) \22> Limit of Borrow Zone 38° -- == 55 ~ — {CO 37! |. on it INDIAN RIVER SHOAL ISOPACHOUS MAP —27°36' —| SURFACE TO BLUE HORIZON +— 27°36' EXPLANATION © Core 4 Survey Line and Navigation Fix ee Scale in Yards 500 250 ) 500 1000 Figure 35. Sediment Thickness between Water-Sediment Interface and Blue Horizon in Central Part of Shoal. 65 potential sources for sand fill (Figure 25). Core 50 in the long north- westerly trending shoal between St. Lucie and Capron Shoal contains excellent material in the upper 4 feet. Cores 67, 68, and 83 from a nameless shoal 6 miles northeast of Fort Pierce Inlet recovered Type A sand to a depth of about 6 feet. Core 87 in another nameless shoal extending northeastward from Fort Pierce Inlet contained 5 feet of suitable material. Except for Thomas Shoal, there are no large shoals between Fort Pierce grid and Canaveral Bight. Since the reconnaissance lines cover- ing this area are all close inshore, no data is available on Thomas Shoal. Cores from the Fort Pierce-Cape Kennedy reconnaissance lines are for the most part devoid of material suitable for beach fill. Only core 181 south of Sebastian Inlet contains material of possible value - a 2-foot layer of coarse quartzose sand overlain by about a foot of silty sand. South of Fort Pierce grid only two cores were obtained between the grid and Palm Beach. One of these - core 55 - located near the landward base of Pierce Shoal contains about 8 feet of good Type A material. Data elsewhere on Pierce Shoal and on three other large shoals of the Fort Pierce-Palm Beach reconnaissance areas - St. Lucie and Gilbert Shoals and an unnamed shoal 4 miles east of St. Lucie Inlet - is lacking. By analogy with the grid area these shoals are expected to be good prospects which warrant further investigation. Although the shoal areas are the most favorable sites for borrow, suitable Type A sediment is widely distributed between shoals in the form of a thin blanket deposit. Effects of exploitation of offshore deposits for large volume supply is presently under investigation. 66 Section V. SUMMARY Between Palm Beach (26°48'N) and Cape Kennedy (28°27'N) the south- eastern Florida Coast is bordered by a submerged plain extending to the top of the Florida-Hatteras slope. The top of the.slope occurs at about -80 feet MLW and 2 miles offshore near Palm Beach, and at about -230 feet MLW, 38 miles offshore at its widest point south of Cape Kennedy. Based on coastal well logs and seismic reflection records, strata underlying the submerged plain to -500 feet MLW are judged to range from Eocene to Holocene in age. These strata all dip generally eastward, but below a presumed unconformity ranging in depth from about -140 to -220 feet MLW, strata dip southeastward and the rate of dip is nearly doubled. The surface of the Shelf plain is topographically divisible into a narrow sloping shoreface, inner and outer Shelf zones and the Shelf marginal zone. The Shelf margin and outer Shelf have irregular surface topography and many indications of "'rocky'" bottom. The inner shelf is mostly mantled by unconsolidated sediments forming many shoal ridges and hills interspersed with relatively flat areas. The shoreface consists mainly of a sloping sedimentary apron connecting the Shelf plain and the littoral zone. Shallow subbottom strata beneath the Shelf surface appear on siesmic profiles as thinly bedded and generally parallel to one another. Internal bedding features are common and usually consist of high and low angle sea- ward dipping bedding planes. The uppermost continuous reflector dips from about -40 feet MLW under the shoreface to apparent outcrop around -65 feet. Cores penetrating to the reflector level indicate that it is composed of variable carbonate sediments with locally lithified layers. This unit is tentatively dated as pre-late Wisconsin. Sediments above the upper continuous and regional reflector reach a maximum thickness of 30 feet under shoals, and thin to as little as 1 foot over flats and swales between shoals. In limited areas on the inner Shelf (i.e., -40 to -70 feet MLW) and in most places on the outer Shelf (-70 feet MLW to Shelf edge), there is no sediment cover over the continuous reflector. The sediment mantle of the inner Shelf consists primarily of sand, silty sand, and shell gravel. Main constituents of this sand are calcium carbonate skeletal fragments; ooids and quartz are the most important secondary constituents. Sediment on beaches adjacent to the study area consists of quartzose sand and shell fragments, the latter generally broken, well-rounded and polished. Median size of midtide samples generally lies in the 0.3 to 0.5 mm (1.74 to 1 phi) range. Surficial sediments in the Fort Pierce grid area between the 40 and 60-foot water depth contours consist primarily of coarse, brown shell sand forming an irregular blanket deposit varying in thickness from 67 1 foot to at least 10 feet, and possibly as much as 30 feet. Thickness of the deposit is closely related to topography, being at a maximum under topographic highs. Most of the sand in the surficial layer, Type A, is usable for beach fill on adjacent beaches, but the characteristics vary considerably. The best material can be obtained only by selective borrow. Sand suitable for beach restoration exists on Bethel Shoal (minimum volume 16.5 x 10 cubic yards); Capron Shoal (minimum volume 65.4 x 10® cubic yards) and the middle section of Indian River Shoal (minimum volume 10.3 x 10 cubic yards). Good material is indicated in a northwesterly trending shoal between Capron and St. Lucie Shoals, in an unnamed shoal lying 6 miles northeast of Fort Pierce Inlet, and in an unnamed shoal extending northeast from Fort Pierce Inlet. By analogy, Pierce Shoal, St. Lucie Shoal and Gilbert Shoal are considered good prospects for beach fill even though direct evidence is lacking. Some shelf material seaward of 70-foot water depth may be suitable for borrow. However, careful survey of potential borrow sites is needed because of the large number of indurated strata in these deeper water deposits and the variable extent and thickness of unconsolidated strata. Shelf sediments in the grid area are judged to be largely relict, and little active sedimentation now takes place outside the shoreface, i.e., beyond -40 feet MLW. Rate and volume of sediment generated by the benthic fauna is not known. Sand removed from the shelf is not likely to be replaced quickly nor by sand-sized material from sources outside the grid. 68 LITERATURE CITED Abbott, R. T. (1954), American Seashells, Von Nostrand, Princeton, N. J. Abbott, R. T. (1968), Seashells of North America, Golden Press, New York. Bermes, B. J. (1958), ''Interim Report on Geology and Groundwater Resources of Indian River County, Florida" Florida Geological Survey, Informa- tion Circular 18. Brown, D. W., Kenner, W. E., Crooks, J. W. and Foster, J. B. (1962), "Water Resources of Brevard County, Florida'', Florida Geological Survey, Report of Investigations No. 28. Bruun, P., Gerritsen, F., Morgan, W. H. (1958), Florida Coastal Problems, Proceedings, 6th Conference on Coastal Engineering, The Engineering Foundation. Cooke, C. W. (1945), "Geology of Florida'', Florida Geological Survey Bulletin 29. Curray, J. R. (1964), "Transgressions and Regressions", Robert L. Miller Papers tn Marine Geology, MacMillan Co., New York. Curray, J. R. (1965), "Late Quaternary History, Continental Shelves of the United States", The Quaternary of the Untted States, H. E. Wright, Jr. and D. G. Frey, Editors, Princeton University Press. De Palma, J. R. (1969), ''A Study of Deep Ocean Fouling, Straits of Florida and Tongue of the Ocean 1961 to 1968", U. S. Naval Oceanographic Office, Washington, D. C. I. R. No. 69-22. Duane, D. B. (1968), Sand Inventory Program in Florida, SHORE AND BEACH, Vol. 36, No. 1. Duane, D. B. and Meisburger, E.P. (1969), "Geomorphology and Sediments of the Nearshore Continental Shelf, Miami to Palm Beach, Florida", U. S. Army Coastal Engineering Research Center Technical Memorandum No. 29. Du Bar, J. R. (1958), "Stratigraphy and Paleontology of the Late Neocene Strata of the Caloosahatchee River Area of Southern Florida", Florida Geological Survey, Geology Bulletin No. 40. Du Bar, J. R. (1962), ''Neocene Biostratigraphy of the Charlotte Harbor Area in Southwestern Florida'', Geological Survey Bulletin 43. Fenneman, N. M. (1938), Phystography of the Eastern Untted States, McGraw- Hill Book Co. Inc., New York. 69 Friedman, G. M. (1964), "Early Diagenesis and Lithification in Carbonate Sediments", Journal of Sedimentary Petrology, Vol. 54, No. 4. Giles, R. T. and Pilkey, O. H. (1965), "Atlantic Beach and Dune Sediments of the Southern United States", Journal of Sedimentary Petrology, Vol. 35, No. 4. Ginsburg, R. N. (1957), "Early Diagenesis and Lithification of Shallow- Water Carbonate Sediments of South Florida'', Regional Aspects of Carbonate Deposits, R. J. Blanc and J. G. Bruding, editors, Society of Paleontologists and Mineralogists Special Publication No. 5. Hall, J. V. (1952), "Artificially Nourished and Constructed Beaches", U. S. Army Corps of Engineers, Beach Erosion Board, Technical Memorandum No. 29. Hathaway, J. C. (1966), "Data File Continental Margin Program, Atlantic Coast of the United States", Vol. 1, Sample Collection Data, Woods Hole Oceanographic Institution, Ref. No. 66-8. Heezen, B. C., Tharp, M. and Ewing, M. (1959), "The Floors of the Oceans; Part 1, The North Atlantic", Geological Soctety of Amertea, Special Paper 65. Henry, D. P. (1958), 'Intertidal Barnacles of Bermuda", Journal of Marine Research, Vol. 17. Kirtley, D. W. and Tanner, W. F. (1968), 'Sabellariid Worms: Builders of a Major Reef Type'', Journal of Sedimentary Petrology, Vol. 38, No. l. Krumbein, W. C. and James, W. R. (1965), "A Lognormal Size Distribution Model for Estimating Stability of Beach Fill Material", U. S. Army Coastal Engineering Research Center, Technical Memorandum No. 16. Lichtler, W. F. (1960), ''Geology and Ground-Water Resources of Martin County, Florida", Florida Geological Survey Report Inv. No. 23. Mauriello, L. J. (1967), "Experimental Use of Self-Unloading Hopper Dredge for Rehabilitation of an Ocean Beach", Proceedings, WODCON, The First World Dredging Conference. Meisburger, E. P. and Duane, D. B. (1969), "Shallow Structural Char- acteristics of Florida Atlantic Shelf as Revealed by Seismic Re- flection Profiles”, Transactions, Gulf Coast Assoetatton of Geologteal Societies, Vol. XIX. Milliman, J. D. and Emery, K. O. (1968), "Sea Levels During the Past 35,000 Years, SCIENCE, December 1968. 70 Moe, M. A., Jr. (1963), "A Survey of Offshore Fishing in Florida", Florida State Board of Conservation, Marine Laboratory, Professional Papers Series No. 4. Morris, P. A. (1951), A Fteld Guide to Shells of our Atlantic and Gulf Coasts, Haughton Mifflin, Boston, Mass. Parker, G. G. (1951), "Geologic and Hydrologic Factors in the Perennial Yield of the Biscayne Aquifer", Journal, Amertcan Waterworks Assoct- tion, Vol. 43, No. 10. Parker, G. G. and Cooke, C. W. (1944), ''Late Cenozok Geology of Southern Florida with Discussion of the Bround Water", Florida Geological Survey, Bulletin No. 27. Perry, L. M. and Schwengle, J. S. (1955), "Marine Shells of the Western Coast of Florida’, Paleontological Research Institute, Ithaca, N. Y. Pilkey, O. H., Blackwelder, B. W., Doyle, L. J., Estes, E. and Terlecky, P. M. (1969), Aspects of Carbonate Sedimentation of the Atlantic Continental Shelf of the Southern United States, Journal of Sedimen- tary Petrology, Vol. 39, No. 2. Pilkey, ‘0. H. (1968), ''Sedimentation Processes on the Atlantic South- eastern United States Continental Shelf", Maritime Sediments, Vol. 4, No. 2. Puri, H. S. (1953), "Zonation of the Ocala Group in Peninsular Florida" (Abstract), Journal of Sedimentary Petrology, Vol. 23. Puri, H. S. and Vernon, R. O. (1964), "Summary of the Geology of Florida and a Guidebook to the Classic Exposures", Florida Geological Survey, Special Publication No. 5. Ryland, J. S. (1967), "Polyzoa", Oceanography and Marine Biology, Harold Barnes, editor, Vol. 5. Shepard, F. P. (1963), Submarine Geology, 2nd Edition, Harper and Row, New York. Tarver, G. R. (1958) "Interim Report on the Ground-Water Resources of St. Johns County, Florida'', Florida Geological Survey, Information Circular 14. Uchupi, E. (1968), "Atlantic Continental Shelf and Slope of the United States - Physiography’', U.S. Geological Survey Prof. Paper 529-C. U. S. Army Corps of Engineers (1966), "Appraisal Report on Beach Conditions in Florida", U. S. Army Engineer District, Jacksonville, Jacksonville, Florida. 7| U. S. Army Coastal Engineering Research Center (1966), 'Summary Report of Contract DA-08-123 CIVENG-65-67, Change Order No. 1, dated 30 April 1965 and Supplemental Agreement Modification No. 2, dated 29 July 1965. (CERC Geology Branch File, Sand Inventory Florida Phase 1). Vernon, R. O. (1951) "Geology of Citrus and Levy Counties, Florida", Florida Geology Survey Bulletin 33. Watts, G. M. (1953), "A Study of Sand Movement at South Lake Worth Inlet, Florida'', U. S. Army Beach Erosion Board, Technical Memorandum No. 42. Wyrick, G. G. (1960), "The Ground-Water Resources of Volusia, County, Florida", Florida Geological Survey Report Inv. No. 22. Zarudzki, E. F. K. and Uchupi, E. (1968), Organic Reef Alignment on the Continental Margin South of Cape Hatteras, Geological Soctety of America, Bulletin Vol. 79. v2 APPENDIX A SELECTED GEOPHYSICAL PROFILES Appendix A contains line profile drawings of selected seismic reflection records from the Fort Pierce grid area. Fix numbers and point of crossing lines are plotted along the upper margin of the profile. The bottom and all subbottom reflectors are delineated and those reflectors mentioned in the text are identified by letter symbols. All depths are in feet below mean sea level; and based on an assumed sound velocity of 4,800 feet per second in water and 5,440 feet per second in the subbottom. Position of lines and fixes are plotted on Figure 2. 73 Line _| Line | Line 3 Line 5 Line 6 Line 7 i eS a] oO Nn |o 2) 2) io foe) o Ohi a= = = Coy | Qo o-= == = = |i =an|= = = Tt iieaaa unt Tall T ea SO ne im SSS ————————— [ ———> —SS = a fofo RRs ve UMM Se Rea aoniccee Oe URN Hate Kroes ay [ SSRIS iy uD perp 200/- er [ WwW tra} jE uw - 300}- [ EXPLANATION mod (109 = Navigation Fix B= Blue Horizon —_Y = Yellow Horizon ey ee | R = Red Horizon 2000 100° 0 ~2000 40006000 500 LINE U Line 9 ine II ine | aD re) Oo Wo! je} wo fon a 1) Ss x Ce) 2) i) T T T aT ali = Saal aer ale 74 none n 100 200 500 FEET Line 4 in Line 6 ine 7 alo — Tv) oO a [o} vT wo @o (o} wo ~~ Oo N nls + + + + wo wo Tes ive} oO oO oO t Led Se Sy) SS GO) SS SLs S ES a SJ S iS 0 T TI inline T T T Sale T Core 86 400 LS ————_ B = Blue Horizon (Sp pa EXPLANATION PSsiniin $0 = Y = Yellow Horizon R = Red Horizon 0 = Orange Horizon 2000 1000 0 2000 4000 6000 HORIZONTAL SCALE IN FEET 500°“ TINE N 1275 =!280 Ey ko 41285 1290 fo} Irregular Surface R Irregular Surface ee) nm fo} oOo inane ee enn FEET 300 S 8 poe 75 8 © x © os ou mo KR = re) K a) rO a ume) es + + ‘o 3) Pe) ro tO ie) rm rom 9 rm ro re) rm nu iw iS) un === a fo 12, m 0 I T Ur T T T T Tim T =yY —_——— =8 7 ————— ee et See ————————————— 100} ————— R 200}- —__ EXPLANATION 400 1343 = Navigation Fix B = Blue Horizon Y = Yellow Horizon R = Red Horizon 0 = Orange Horizon I ——— — 000 500 LINE A Line | 8 S 8 4 ms iS o |S 3S 8 re) be) 1 9) (a) a) POS: ae) be) T T ls T T T T 4 g —<—— 7 ™ = ———— . Irregular Surface 4 —— — Boy = Y. ———S Q Irregular Surface ih 100 Peale Se ee ae | +200 +300 We +400 = I500 76 fo} 2324 12320 42315 2312 +2305 +2300) 2295/5 ia 412290 - 2289 {2281 100 200 ( ww pet ive Mise 300 [a EXPLANATION to} 400) wale an 5 2312 = Navigation Fix HORIZONTAL SCALE IN FEET —— B = Blue Horizon Y = Yellow Horizon 2000 1000 0 2000 4000 6000 eae R = Red Horizon O = Orange Horizon 500 LINE 4 Ihne 42145 iC e 42140 i E 5 (ee i kn 42130\- i : : 42125 (c Ie 42120 lo} fon Loin nL penn en peepee ay 77 100 200 FEET 300 400 500 FEET Line A ni ° nif re) ° re) ° 79) ft wo o oO =~ ia oO @o oO jo 2 2 oS 2 2 2 io Olam FI =U T T T T ali 100+ L en rrel 200} 300 Rages 0 sae memes eer } a a SS [ EXPLANATION soCl 1980 = Navigation Fix HORIZONTAL SCALE IN FEET i" B = Blue Horizon Y = Yellow Horizon 2000 51000 as 0 as ooo Gao L R = Red Horizon 0 = Orange Horizon 500 LINE 13 in @o fo} wo [e} NI Tt wo wo Mm [e} @o wo @ fez) fon) fo} [e) (oy (2) feo} oOo @ med ~ fon) fon) fon) fo} Oo (oy (es) fon) a fon) a aD =_ _ = N N N N N N N N N al mle T T T T T T T 2974 2960 +2956 2955 2950 2970 +2965 296 78 APPENDIX B GRANULOMETRIC DATA Appendix B contains the results of size and acid solubility analysis of selected samples from the study area. 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ATV 82 Percent Coarser SIZE ANALYSIS Millimeters 3250) 12:50 1.50 “90.10, FOS2s Hn So, .25 5 09 07 x : . 8 60] .50| 40] .3 V Lie aa Ora sa (=i Plies: ciate a ig ct a Fei i ea al 2.0 -I.5 -1.0 -0.5 to) 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 Phi Units @ 4 VERY COARSE VERY FINE WENTWORTH SCALE Graphic size distribution curves for a typical sample from Indian River Shoal and a nearby beach area (dashed line). Location of samples is shown on Figure 2 and 25. 83 Percent Coorser SIZE ANALYSIS mimes oolre Gee ; TTT AT 62 2.0 -1.5 <-10 -0.5 0.5 1.0 1.5 2.0 2.5 3.0 3.5 Phi Units @ GRANULE | VERY COARSE | CoARSE SAND | MEDIUM SAND | FINE SAND VERY FINE WENTWORTH SCALE Graphic size distribution curves for typical samples from Bethel Shoal and from a beach in the northern part of Fort Pierce Grid area (dashed line). Size distribution of the acid insoluble residue (mostly quartz) for one of the shoal samples is also included. Location of samples is shown on Figures 2 and 25 84 Percent Coarser SIZE ANALYSIS p Millimeters 3.50 2.50 1.50 90 .70 .55 .45 .35 .25 5 (OSREO” : J -80] 60] .50] 40] .2 10] .08 Ae A : : 98 38 y pide |e W/ be oseeqatlbe Gils YJ 1 | LA 5 | Bali Alveinba ehrexs bvis}izdaph oi 60 a Fe es ; 2 | eepensd pe oe es aes re ee 30 fae Be vas Uh ls naa wi r ee a er a Ht Cy ae ie fo eype a4 Mi kecdlanam ls ee 5 L / I 4 3 120 -|.5 <-1.0 -0.5 {0} 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0 i Phi Units @ WENTWORTH SCALE Graphic size distribution curves for typical samples from Capron Shoal and a nearby beach (dashed line). Location of samples is shown on Figures 2 and 25. 85 APPENDIX C SEDIMENT DESCRIPTIONS Appendix C contains visual description of sediments contained in cores from the study area. Core number, CERC identification number, and sample depth in core are listed to the left. Visual descriptions are based on both megascopic and microscopic examination. The descriptive statement generally contains (in order) the following elements: i Color 2. Color code per Munsell Soil Color Charts (1954 edition)* 3. Dominant size or size range. 4, Major compositional element or elements with the dominant constituent listed first. 5. Phrases identifying readily recognized constituent elements with an estimated frequency of occurrence in terms of total particles. The frequency terms indicate the following percentages: a. Profuse, 30-50% of total particles b. Common, 10-30% of total particles c. Sparse, 2-10% of total particles d. Trace, less than.2% of total particles. 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REPORT TITLE GEOMORPHOLOGY AND SEDIMENTS OF THE INNER CONTINENTAL SHELF, PALM BEACH TO CAPE KENNEDY, FLORIDA 4. DESCRIPTIVE NOTES (Type of report and inclusive dates) 8. AUTHOR(S) (First name, middle initial, last name) Meisburger, E. P. Duane, D. B. 6. REPORT DATE 7a. TOTAL NO. OF PAGES 7b. NO. OF REFS February 1971 Ly 4l 8a. CONTRACT OR GRANT NO. 9a. ORIGINATOR’S REPORT NUMBER(S) DA-08-123-CIVENG-65-57 between Alpine b. PRosectNo. Geophysical Associates and Coastal Engineering Research Center. Technical Memorandum No. 34 9b. OTHER REPORT NO(S) (Any other numbers that may be assigned this report) 10. DISTRIBUTION STATEMENT This document has been approved for public release and sale; its distribution is unlimited. 11. SUPPLEMENTARY NOTES 12. SPONSORING MILITARY ACTIVITY 13. ABSTRACT The Inner Continental Shelf off eastern Florida was surveyed by CERC to obtain information on bottom morphology and sediments, subbottom structure, and sand deposits suitable for restoration of nearby beaches. Primary survey data consists of seismic reflection profiles and sediment cores. This report covers that part of the survey area comprising the inner Shelf between Palm Beach and Cape Kennedy. Sediment on beaches adjacent to the study area consists of quartzose sand and shell fragments. Median size of midtide samples generally lies in the range between 0.3 to 0.5 mm. (1.74 to 1.0 phi) diameter. The Shelf in the study area is a submerged sedimentary plain of low relief. Ridge-like shoals generally of medium-to-coarse (0.25 to 1.0 mm.) calcareous sand resting on the seaward dipping subbottom strata contain material suitable for beach restoration. A minimum volume of 92.2 x 106 cubic yards of suitable sand is avail- able within study limits. REPLACES DO FORM 1473, | JAN 64, WHICH 18 D feel 47 CESOC ET EITC RIARMYAU Se UNCLASSIFIED Security Classification UNCLASSIFIED Security Classification KEY WORDS Submarine Geology Continental Shelf Seismic Reflection Sediment Cores Artificial Beach Nourishment Palm Beach-Cape Kennedy, Florida UNCLASSIFIED Security Classification “aTqeTTeAe st spzeX 9TqQNd oOT X 72°26 JO OWNTOA uUMUTUTW “TTTF YyoeVeq IOJ aTqejINs TeTIo},eW UTeUOD ejeIXS wojjoqqns Sutddtp paremess oy} uo BuTJSoL sTeOYS ayxT[-9Bpty ‘Fotos MoT Jo uteTd AzrejUoUTpes pes1ouqns e sT vote FToyS ‘zLojyowetp (tyd O'T 02 pl'T) ‘ww s*Q 02 ¢'°0 WOLZ FO SBueI dy} UT seTT ATTeLoUes soTtdwes OPTIpPl FO 9ZTS UeTPeW “S}USWBeIFZ [TTeys pue pues 9sozjrenb Fo sjsts -u0d JUSUTpas YyOeeg ‘se10D JUsWTpas pue seTtyord uotjIeTFeL Itustas Fo s}stsuod eqep Aoaans Areutig ‘*TITJ yoreq oJ eTqeiIns sytsodap pues pue *9mn}9nI4s wojOGqns ‘sjUsUTpes pue AZoToydIow woj.OqG UO UOTEeULIOFUT ute qo 03 peXkdsaAIns sem BPTIOTY uLaqysea FFO FTAYS Te USUTIUOD ToUUT sy] "gd ‘qd ‘oueng ‘III da IdISSVIONN vS “ON WNGNVYOWAN IVOINHOSL ‘d ‘g ‘aeBanqstow ‘II ia — Car IZ61 Azenigay ‘sextpueddy ¢ pue setqel ¢ eptsoty ‘ Apouusy ‘serin3ty s¢ 3utpntout sesed pIT[T ‘eueng ‘gq ‘Ga edej - yoeog wieq °S pue resainqstew *q “gy Aq WAINOTA * AGANNAY JuUSWYSs TINON AdVD OL HOVAd W1Vd ‘ATAHS IVLNANILNOO yoeog TetoTFTI4zy “Pp YANNI JHL dO SLNAWIGES ANV ADOTOHdYONOSD 91002 ‘9 ‘d ‘NOLONTHSYM ‘dD “YFLNIO HOUVASHY OYONA TVLSVOD AWYVY *S ‘/N “oTqeTteae St spteA DTGND OT X 7°26 JO oUMTOA uMUTUTW ‘“TITJ Yoeeq TOF O9TqejINs [ettojJew utTeJUOD e4eIAS wozjoqqns Sutddtp paiemess oy} uo BUTJSeI STBOYS OYXTT-esptyY “JotpToes MOT Jo utetd AzeJUsWTpes peSxrowgns e st wore JTayS ‘1ajouetp (tyd O'T 07 pLZ'T) ‘wu s‘Q 03 ¢'0 Woz FO OBueI dy} UT SaTT AT[eLeUes soatdues OpTIPTU FO OZTS UeTPpaW ‘SjUsWSeIZ T[TaYys pue pues asozjIenb Fo systs -uOD JUOdIITpss yoeeg ‘Sd1OD JUsUTpes pue seTTjford uotIeTJeI Itustes jo S}STsuod eiep AdAINS AIeUTIg ‘[ITF yoeeq TOF aTqejIns sztsodep pues pue *ganjzonz7zs wojOGqns ‘sjueUTpes pue AZoToydzow wojOqG UO UOT}eWIOFUT ute igo 0} peksAIns Sem BPTIOT A ulajsea JJO FJTeys Te JUeUTJUOD TouUl syL ‘a ‘a foueng ‘III ddIdISSVIONN v ‘ON WAGNVYOWSN TVOINHOSL ‘d ‘g ‘zesanqstow “II Ora, Pt IZ61 Azenaqey ‘sextpueddy ¢ pue setqel ¢ eptioty ‘ Apouusy ‘soin3ty s¢ Zutpntout soesed pIT ‘oueng ‘gq ‘a eden - yoeog wIeq “Ss pue zesanqstow *d “gd Aq VGINOTA ‘ AGHNNAY JUSWYSTINON adVO OL HOVSd WIVd ‘A THHS TVLNSNILNOO yoeog TeTOTFTIIy * YANNI dHL dO SLNAWIGHS GNV ADOTOHdYONOAD $e10) USUTpess ° UOTJIOTFOY OTWsTISs ° ABoTos9 eutzrewqns ° 91002 ‘9 ‘d ‘NOLONIHSYM “dO “YdLNSD HOUVASTY OYONT TVLSVOD AWYV “S “A aAANM t+ ‘oTqe[teae st sparek 9TqGnd oOT X 2°26 FO OUNTOA wNUTUTW “TITTF YOeeq TOF STqQejINS TeTIojeU UTeUOD BIeIXS wojjoqqns Butddtp pxremess dy} UO BUTJSOeL S[TeOUS aYT[-esply ‘Fatper Moy Jo uteTd Azequoutpes pasreuqns e ST vole JToeyg ‘seqzoweIp (tud Q'T 02 pL'T) ‘ww S*'Q 03 ¢°Q WoOIZ Fo 9BueXI dy. 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