& Ac : ‘ ava (Ne TP 81-3 Sand Resources and Geological Character of Long Island Sound by WHO] . DOCUMENT S. Jeffress Williams \ COLLECTION TECHNICAL PAPER NO. 81-3 MAY 1981 Approved for public release; distribution unlimited. U.S. ARMY, CORPS OF ENGINEERS _ COASTAL ENGINEERING |e RESEARCH CENTER i Kingman Building Vg), f= Fort Belvoir, Va. 22060 Ws Any Cai Gag, Nee. ele Te TP 81-3 Sand Resources and Geological Character of Long Island Sound by S. Jeffress Williams TECHNICAL PAPER NO. 81-3 MAY 1981 Approved for public release; distribution unlimited. U.S. ARMY, CORPS OF ENGINEERS COASTAL ENGINEERING Me RESEARCH CENTER i Kingman Building | 1), f= Fort Belvoir, Va. 22060 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 has been made by this Center. Additional copies are available from: National Technical Information Service ATTN: Operations Diviston 5285 Port Royal Road Springfield, Virginia 22161 Contents of this report are not to be used for advertising, 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. UNCLASS IFIED SECURITY CLASSIFICATION OF THIS PAGE (When Data Entered) READ INSTRUCTIONS T. REPORT NUMBER 2. GOVT ACCESSION NO,| 3. RECIPIENT'S CATALOG NUMBER TP 81-3 4. TITLE (and Subtitle) 5. TYPE OF REPORT & PERIOD COVERED Technical Paper SAND RESOURCES AND GEOLOGICAL CHARACTER OF LONG ISLAND SOUND 6. PERFORMING ORG. REPORT NUMBER 8. CONTRACT OR GRANT NUMBER(s) 7. AUTHOR(S) S. Jeffress Williams 10. PROGRAM ELEMENT, PROJECT, TASK AREA & WORK UNIT NUMBERS D31665 12. REPORT DATE May 1981 13. NUMBER OF PAGES 65 15. SECURITY CLASS. (of this report) UNCLASSIFIED 9. PERFORMING ORGANIZATION NAME AND ADDRESS Department of the Army au Coastal Engineering Research Center (CEREN-GE) Kingman Building, Fort Belvoir, Virginia 22060 11, CONTROLLING OFFICE NAME AND ADDRESS Department of the Army Coastal Engineering Research Center Kingman Building, Fort Belvoir, Virginia 22060 14. MONITORING AGENCY NAME & ADDRESS(if different from Controlling Office) DECL ASSIFICATION/ DOWNGRADING SCHEDULE 15a, 16. DISTRIBUTION STATEMENT (of this Report) Approved for public release; distribution unlimited. DISTRIBUTION STATEMENT (of the abstract entered in Block 20, if different from Report) - SUPPLEMENTARY NOTES - KEY WORDS (Continue on reverse side if necessary and identify by block number) Beach nourishment Sand and gravel resources Geomorphology Sediments ICONS Seismic reflection profiles Long Island Sound Shore restoration ABSTRACT (Continue on reverse side if necesaary and identify by block number) Long Island Sound, covering almost 3,400 square kilometers of the region between Long Island, New York, and the Connecticut mainland, was studied using 700 kilometers of high-resolution seismic profiles and 75 vibratory cores to determine the geologic character and Quaternary history and evolution of the Sound, as well as to assess the resource potential of sand and gravel in sea- floor deposits. (continued) DD en, 1473 Evrtion oF 1 now 6546 OBSOLETE UNCLASSIFIED SECURITY CLASSIFICATION OF THs PAGE (When Data Entered) UNCLASS IF LED SECURITY CLASSIFICATION OF THIS PAGE(When Data Entered) The subbottom consists of igneous and metamorphic bedrock that crops out close to the Connecticut shore and slopes south to depths of -250 meters at the Long Island north shoree The bedrock surface under the Sound is highly irregular and exhibits relief on the order of +30 meters. There are numerous buried river channels that generally trend north-south in the western Sound, and apparently project south under Long Island; a large east-west channel along the long Island north shore that underlies eastern long Island and Gardiners Bay, projects south to possibly join the Block Island Shelf channel. Many channels, deeply scoured by Pleistocene glaciers, project south from present-day rivers along the Connecticut shoree The deepest channel at -244 meters MSL underlies New Haven Harbor and trends southwest past a bedrock high at Stratford Shoal and then projects south under the Long Island mainland. Cretaceous strata overlie the bedrock in isolated areas of the middle of the Sound and exhibit considerable surface relief due to erosion by multiple glacial advances. Pleistocene sediments consist of thick accumulations of very firm varvelike silts and clays filling and overlying the bedrock surface throughout much of the central Sound, as well as moderately to poorly sorted sands and gravels up to boulder size that were placed as discontinuous reces— sional moraine segments, glacial outwash heads, and fluvial deltas. The pres- ence of these glacial depositional features on the seabed from the western end of the Sound to about the Connecticut River longitude is evidence for one or more readvances of the late Wisconsin glacier subsequent to deposition of the Harbor Hill Moraine rimming the Long Island north shore. Holocene sediments consist primarily of organic sandy muds that are accumulating in low energy environments. The primary sources of these fine- grained materials are coastal erosion of glacial debris, riverine inputs, and landward transport of fines from adjacent Block Island Sound and the inner shelf. Fourteen isolated shoal features have been identified as offering the highest potential as sources of beach-fill sand and construction aggregate. Based on available data, a conservative estimate is that 189 million cubic meters of sand and gravel is available in water depths not exceeding 20 meters if the latest dredging technology were used. 2 UNCLASS IFIED SECURITY CLASSIFICATION OF THIS PAGE(When Data Entered) PREFACE This report describes results of the Inner Continental Shelf Sediment and Structure (ICONS) study of Long Island. The primary objectives of the study were to locate and delineate offshore sand and gravel deposits suitable for beach nourishment and to provide information on the geologic character of Long Island Sound. The work was carried out under the coastal processes program of the U.S. Army Coastal Engineering Research Center (CERC). The report was prepared by S. Jeffress Williams, a CERC research geolo- gist, under the general supervision of Dr. C.He Everts, Chief, Engineering Geology Branche As part of the research program of the Engineering Develop- ment Division, the ICONS study is under the general supervision of N. Parker, Chief of the Division. The fieldwork (involving coring and continuous seismic profiling) was accomplished under contract with Alpine Geophysical Associates, Ince Discussions with E.P. Meisburger (CERC) were helpful in preparation of the study; final manuscript reviews by E.Pe Meisburger and Dre C.H» Everts were appreciated. Microfilm copy of all seismic data is stored at the National Solar and Terrestrial Geophysical Data Center (NSTGDC), Rockville, Maryland 20852. Cores collected during the field survey program are in custody of the Univer- sity of Texas, Arlington, Texas 76010, under agreement with CERC. Requests for information relative to these items should be directed to NSTGDC or the University of Texas. Comments on this publication are invited. Approved for publication in accordance with Public Law 166, 79th Congress, approved 31 July 1945, as supplemented by Public law 172, 88th Congress, approved 7 November 1963. Colonel, Corps of Engineers Commander and Director CONTENTS Page CONVERSION FACTORS, UeS. CUSTOMARY TO METRIC (SI)cccccccccccecce 8 I INTRODUCTION. cccccccccccccvcccccccc cess cc cose ceec cv ec ccc ee eseole 9 1. Backgroundecccccccccccccccccccccccccccceesevceccececsvcccce 9 2. Field and Laboratory ProcedureSececccccceccccccccccecccccce 10 3. SCOPCecccccccccccvcccccccvcccccccccccccscccecscccccccsccccces§ 12 4. Geographic and Geologic Settingeccccsccccccsccccccccvsccccce 13 5. General Stratigraphy of Long Island and Connecticut........ 13 Ge Bathymetryccocccccccccccccccccvvcccccceccccccccscccccccccccs §« 16 7- Previous Geologic InvestigationSercccccercccccccecccccccccce 1/ Il GEOMORPHOLOGY AND SHALLOW SUBBOTTOM CHARACTEReecccccccccccccccce 21 1. Shallow Subbottom Structure and Stratigraphyeoeccsccsccccccce 21 2. Surface and Subbottom Sediment Character and Distribution... 32 IIl BEACH-FILL NEEDS AND RESOURCE POTENTIAL. cccccccccccccceccccsccvcce 30 1. Sandfill Requirements for Long Island and Connecticut Beacihive'lsleteleleictelelchelotolelcleiclelelolclolelcis cleloveloleleieloleheicleleloreiclcrelcroiciole clelere 36 2. Suitability of Sand for Beach Nourishmentececcccecccccccccee 3/ 3. Primary Sand and Gravel! DepoSitse..ccccccccccesccscccccccses 36 IV SUMMARY 4etoleloleleleioheisnsieleielsloteleleleielelelotelelcioleloleleleleleleletelelelolerelercloleioleleveleieierelere 51 LITERATURE Cali D efetereteleiclololovelelelolclolololelelcieloheliclcherciclololeleleierciovelcieleleneieterchere 53 APPENDIX A CORE SEDIMENT DHOGREMP AMON S erclelakelelioielorshelelekoiolelcleleioioiololelelerehoiclolelereleioroiere 58 B RESULTS OF GRAIN-SIZE AINAUEN(SaltStetetslololelelelotelelelsreiohereroreloveneleieicreneverctenetetels 63 TABLES 1 Generalized stratigraphy of Long Islandewcccccccccccccccccccccccsccccee 15 2 General stratigraphy of Connecticut. .cccccccccccccccsccecscccsccccsccessce 16 3 Summary of Quaternary geologic EveNntSceccccccccccceccccccccccccccccvcce 28 4 Grain-size scales~-soil classification... .ccccccccccccsccccccccccccccess 34 5 Characteristics of sand and gravel depOSitSecccccccccccccccccccccccccee 39 FIGURES 1 Regional map of Long Island Sound showing its relation to the Piedmont province of Connecticut and Atlantic Coastal Plain province of Long SAT tetelevelclololelotoleleloveiclelelcleleleletelelolcvelelelelelolclelcieiereiololeiereietenets We 2 Trackline locations for the high resolution seismic reflection profiles and vibratory cores used in the Studyeoceccccscocccccesccecccee 14 13 14 15 16 17 18 ILS) CONTENTS F IGURES-——Continued Geologic cross section from the south shore of Long Island at Fire Island north across Long Island Sound to the Connecticut mainland.... Bathymetry of Long Island Sound showing the major land and shoal FEAEUTESo acvercrersereye eiclelerc cle cercielelcveieicleve siercleralclecciciclave cieveravace avetetia lore avai cisisieies Cross-sectional profiles of the Long Island Sound sea flooreccecceccee Typical seismic profile off the Norwalk Islands, Connecticute.eccceccce. Photos of apparent varve sediments retrieved in the Orient Point boring drilled into the Orient Point buried channelecccecccccccccccce Map of coastal Connecticut from Branford to Hammonasset Point showing the location and alinement of several shoals and islands determined as remnants of the Madison and Old Saybrook Moraines....e. Map of late Wisconsin-age Harbor Hill and Ronkonkoma Moraines along Long lista disjeietoicleretorcreioleleiolelelelereletelelotereletsioleiciololoretcletelctetaletsrenelereiorerevereie Map of glacial features in eastern Long Island Sounde.ccccccceccccccee. Map of glacial features in the Norwalk Island regioneccccecccccccccccce Typical seismic profile of a glaciated bedrock channel filled with Pleistocene SECIMENTS ce ccccccccccccccscccccccccccccccscccccccccccescce Eighty cores analyzed to show the four primary sediment types present in the top 5 meters of the Sea f1lOOLececceccccccccccecccccccce The cores and seismic profiles used to map the surface sediment distribution of the four primary types in Long Island Sound.....c.ccce Projects along the Connecticut shore involving beach fill. .cccccceccece The 14 primary sand and gravel deposits identified in Long Island SOuMGlS 60000000000000000000005000905000000005000000000000000060000000600 Map of western Long Island Sound showing four deposits and locations of the pertinent seismic and core datdecccccccccccccccccccce Interpreted profile of seismic line 1 of two shoals off Matinicock PONE GOD ODOODDDDO000000000000000000000000000000000000005000000000000 Map of primary deposits E and F along the Connecticut Shoreecccccccoce Page 15 18 19 23 25 26 27 28 30 Sil 33 35 37 38 40 41 42 20 21 22 23 24 25 26 Zi CONTENTS F IGURES-—Continued Interpreted profile of seismic line B-105 crossing area E southeast of the Norwalk TSHland Sloreletoloieialelaislalelelelelelolelelelciclelclelolclelolelclclelelelelelelolciclalereleleie Interpreted profile of line B-22 at the south end of the Lordship outwash head showing forset stratificationecccecceccccceccccccccccccce Map of sand and gravel deposits D and G along the north shore of Long liSiFaincleteleleleleleloleleleselclelelelelclelelelolelelelelelclclelelelelelelololeleleleleloleielelelolelole clelsiclelcle Map of the Long Island north shore from Port Jefferson to Roanoke Point showing potential borrow areas H, J, and Leceeceecececececcccccce Map of deposits I and K near New Haven, ConNeECticuteccccccccccccccccce Map of borrow area M along the Long Island north Shoreeececcecccccccece Map of eastern Long Island Sound showing the morphology of Long Sand ShrOalletelelelelereloletclelclelcteicleiclelelclelclelelelolelclclelcielclolelolejclelelelelelelelelelelelcleleleiekelelels Interpreted profile of seismic line 12la over Long Sand Shoalececececcee Page 43 45 46 47 47 49 50 51 CONVERSION FACTORS, U.S. CUSTOMARY TO METRIC (SI) UNITS OF MEASUREMENT U.S. customary units of measurement used in this report can be converted to metric (SI) units as follows: eS ooeeoeoEoEoEoEooaoaoaoaoaoaoaoao————————————————— Multiply by To obtain inches 25-4 millimeters 2054 centimeters square inches 6.452 Square centimeters cubic inches 16.39 cubic centimeters feet 30.48 centimeters 0.3048 meters square feet 0.0929 square meters cubic feet 0.0283 cubic meters yards 0.9144 meters Square yards 0.836 square meters cubic yards 0.7646 cubic meters miles 1.6093 kilometers Square miles 259.0 hectares knots 1.852 kilometers per hour acres 0.4047 hectares foot-pounds 1.3558 newton meters mribiGiCiinneecs oOlO7 sz Or kilograms per square centimeter ounces 28-35 grams pounds 453.6 grams 0.4536 kilograms ton, long 1.0160 metric tons ton, short 0.9072 metric tons degrees (angle) 0.01745 radians Fahrenheit degrees 5/9 Celsius degrees or Kelvins! 1To obtain Celsius (C) temperature readings from Fahrenheit (F) readings, use formula: C = (5/9) (F -32). To obtain Kelvin (K) readings, use formula: K = (5/9) (F -32) + 273.15. SAND RESOURCES AND GEOLOGICAL CHARACTER OF LONG ISLAND SOUND by S. Jeffress Williams I. INTRODUCTION 1. Background. Ocean beaches and dunes constitute a vital buffer zone between the sea and populated coastal areas, and also provide much-needed recreation areas for the public. The construction, improvement, and maintenance of beaches through the 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, iin, UO SK3} (sell, 52) o Where a specified plan of improvement involves shore restoration and periodic nourishment, large volumes of sandfill may be needed. In recent years it has become increasingly difficult to obtain suitable sand from lagoonal or inland sources in sufficient quantities and at an economical cost for beach-fill purposes. This difficulty is due in part to increased land value, depletion of previously used nearby sources, and added cost of trans-— porting sand from areas increasingly remote. Material composing the bottom and subbottom of estuaries, lagoons, and bays is often too fine grained and unsuitable for long-term protection. Regardless of the fill source, beach sediment seeks equilibrium with its environment. However, it is possible to estimate the amount of material that will be lost through sorting in the surf zone by a quantitative comparison of the placed material with the native material and therefore minimize losses through selection of the most suitable fill material (Krumbein and James, 1965; James, 1974; Hobson, 1977). The problem of locating suitable sand supplies 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 deposits suitable for future beach- fill requirements. This exploration program is conducted through the U.S. Army Coastal Engineering Research Center (CERC). In 1964, a program was initiated to survey offshore regions of the Atlantic, Pacific, gulf, and Great Lakes coastal areas to delineate the character of sand deposits. Formerly called the Sand Inventory Program, it began with a survey off the New Jersey coast. Subsequent surveys have included the Inner Continental Shelf off Florida, Texas, New England, New York, Maryland, North Carolina, Delaware, Virginia, California, and lakes Michigan and Erie. Recognizing a broader application to the CERC mission of information collected in conduct of the research, the program was referred to as the Inner Continental Shelf Sediment and Structure (ICONS) program. The ICONS program was directed not only toward the mapping of sand deposits suitable for beach restoration but also the delineation of shelf structural characteristics, analysis of shelf history and sediment sources (Duane, et al., 1972; Pilkey and Field, 1972; Field, et al., 1979), determination of regional engineering properties of shelf sediments (Williams and Duane, 1972), and effects of ocean dumping (Williams, 1979). An early study by the Corps of Engineers in evaluating techniques for transferring offshore sand to the beach is described by Mauriello (1967). This experiment at Sea Girt, New Jersey, involved dredging of 191,000 cubic meters of sand by the hopper dredge, Geothals, at a location 3.2 kilometers offshore from the beach segment to be restored. The loaded dredge, which had a pumpout capability, docked alongside an anchored barge and the sand was pumped ashore through a submerged pipeline. At Redondo Beach, California, in 1967-68, the U.S. Army Engineer District, Los Angeles, contracted dredging of more than 1.1 million cubic meters of sand from offshore depths of 12 meters and transferring the sand to the beach. These operations, as well as others conducted in open-ocean environments in Long Island Sound and along the gulf and Atlantic coasts, have demonstrated the feasibility of using offshore marine and lake deposits for beach nourish— ment operationse Along the Connecticut shore alone, about 32 kilometers of beaches have been filled and nourished from about 1940 to 1970 by using hydraulic dredges to pump material to the beaches from offshore source areas (McCabe, 1970). The projects were cooperative efforts between the Corps of Engineers, the State of Connecticut, and the individual towns along the shore. In some cases the fill sand was derived from navigation channel dredging, but more often it was obtained from borrow pits close to the project beaches. 2. Field and Laboratory Procedures. The exploration phase of the ICONS program uses seismic reflection pro- filing supplemented by cores of the bottom sediment. Supporting data for the studies are obtained from National Ocean Survey (NOS) hydrographic smooth sheets and from literature sources. Planning, seismic reflection profiling, coring, positioning, and analysis of sediment obtained in the cores are detailed in Williams and Duane (1974). A brief description of these tech- niques follows: ae Planning. Survey tracklines were laid out initially in grid or reconnaissance linese A grid pattern (line spacing of about 4 to 5 kilo- meters) was used to cover areas where a more detailed development of bottom and subbottom conditions was desired. Selection of core sites was based on a continuing review of the seismic profiles as they became available during the survey. This procedure allowed core-site selection based on the best information available; it also permitted the coring to be completed in one area before coring was started at another site. be Seismic Reflection Profiling. Seismic reflection profiling is a technique for delineating subbottom structures and bedding planes in sediments and rocks underlying water-covered arease Continuous reflections are obtained by generating repetitive, high-energy sound pulses underwater near the water surface and recording “echoes” reflected from the bottom-water interface, and subbottom interfaces beween acoustically dissimilar materials. In general, compositional and physical properties which commonly differentiate sediments and rocks also produce acoustic contrasts. Thus, an acoustic profile is roughly comparable to a geologic cross sectione 10 Seismic reflection surveys of marine areas are made by towing sound- generating sources and receiving instruments behind a survey vessel which follow predetermined survey tracklines. For continuous profiling, the sound source is fired at a rapid rate, and returning signals are amplified and fed to a recorder which graphically plots the two-way signal traveltime. Assuming a constant speed for sound in water and shelf sediments, a vertical depth scale can be constructed to the chart paper. Horizontal location is obtained by frequent (2-minute intervals) navigational fixes keyed to the chart record by an event marker. General seismic profiling techniques are discussed in Moore and Palmer (1968) and American Association of Petroleum Geologists (1977). Seismic reflection profiles for this study were made with an engineering “sparker" (Alpine Geophysical Associates, Inc., 1965). Two sound sources, one operated at 100 joules and the other at 200 joules, were fired alternately at a pulse rate of 4 per second during the survey. Returns from the sound sources were recorded by a dual-channel recorder which displayed the results on a single strip chart. ce Coring Techniques. An Alpine Geophysical Associates, Ince pneumatic, vibrating hammer-driven coring assembly was used to obtain cores from the survey area. The apparatus consists of a standard 5-meter-long core barrel, acrylic liner, and shoe and core catcher, with the driver element fastened to the upper end of the barrele These are enclosed in a self-supporting frame which allows the assembly to rest on the bottom during coring, thus not influ- enced by 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 contain- ing the cored material is removed and capped. Denser materials (compact sands; partially lithified rocks) are more difficult to penetrate than loose materials. Cohesive materials cause drag on the liner walls and give some distortion. de Navigation. Position location was determined during the survey by use of the Decca Navigator Mark 12 Receiver and Track Plotter which accurately located the vessel with respect to two onshore reference points. Navigation fixes were made at 2-minute intervals during all seismic reflection survey work and at each core position. Final plots of trackline and core location compiled from survey data were prepared at scales of 1:80,000. e. Processing. Seismic records were analyzed to establish the principal bedding, erosional, constructional, and structural features in upper subbottom strata. After preliminary analysis, typical records were reduced to detailed cross-sectional profiles showing all reflective interfaces within several hundred feet of the bottom. Selected reflectors, considered significant because of their extent and relationship to the general structure and geology of the study area, were then mapped. If possible, the uppermost mapped reflector was correlated with core data to provide a measure of continuity between cores. Cores were visually inspected and logged aboard ship. After delivery to CERC, the cores were sampled every foot by drilling through the liners and removing samples of representative material. After preliminary analysis, a number of representative cores were split to determine details of the bedding. 1l Cores were set up for splitting in a wooden trough. A circular powersaw mounted on a base which is designed to ride along the top of the trough was set 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° segment of the liner was cute The sediment above the cut line was then removed with a spatula, the core logged, sampled, and photographed. Samples from cores were examined under a binocular microscope, and de- scribed in terms of gross lithology, mineralogy, and the type and abundance of skeletal fragments of organisms. Petrographic analysis through transmitted- light microscopy was performed on certain core samples that coincided with prominent acoustic reflectors to further delineate their nature and origin of associated sediments. Data processing included analysis of all seismic reflection records and reduction to line profile drawings. Cores were logged and sampled to provide sediment representative of each sediment facies penetrated. The samples were visually described and size analysis was made by means of a fall velocity-type rapid sediment analyzer. The positions of cores and seismic reflection pro- file lines were also plotted at a scale of 1:80,000. 3. Scope. This study concentrates on the geologic character of the subbottom and sediment distribution over most of Long Island Sound which covers nearly 3,400 square kilometers of the region between Connecticut and Long Island, New York (Fig. 1). The study area extends from Fishers Island (72°00' W.) on the east to near the East River (73°45' We.) on the west, close to New York City. Because of the nature of this study, area emphasis is on the nearshore parts of the Sound along the shores of Connecticut and northern Long Island in water depths from 3 to 30 meters; the central parts of the Sound at the eastern and western ends are also covered in some detail. Bane \ wWESTONES TER nD Island GoUN TY SS 5 o ¥ TF wks Fe, a Mourauk Point Or Nore ath € eee NoneAA Lloyd Point BRONX ‘ ee NASSAU ‘; COUNTY \ Figure 1. Regional map of Long Island Sound showing its relation to the Piedmont province of Connecticut and Atlantic Coastal Plain province of Long Island. ly, The field data used in this study consist of continuous seismic reflection profiles and vibratory cores shown in Figure 2. The data were collected in 1967 under contract with Alpine Geophysical Associates, Imc., and consist of 700 kilometers of sparker trackline acoustic profiles and 75 cores, 9 centi- meters in diameter and a maximum of 5 meters longe The lengths of actual sediment recovered in the cores range from 1.3 to 5 meters. These primary data were supplemented by numerous reports in the technical literature and by use of the NOS 1:80,000-scale charts. 4. Geographic and Geologic Setting. Long Island Sound, one of the largest estuaries on the east coast of the United States, has a general east-west orientation and is about 180 kilometers long with a maximum width of 45 kilometers in the center and narrows at both ends to about 18 kilometers wide. One of several basins that occupy the New England part of the Atlantic Coastal Plain province, it lies at the contact boundary between the crystalline Piedmont rocks and the Cretaceous Coastal Plain strata. Like the other basins to the east (Block Island Sound, Rhode Island Sound, Nantucket Sound, and Buzzards Bay), Long Island Sound is bounded on the south by till deposits from the southernmost terminus of the continen- tal glaciers which occupied the region in the Pleistocene epoch. The Connecticut coast of Long Island Sound is highly irregular with numerous embayments, islands close to shore, and coarse-grained sandspits and beaches. The coast is very rocky, dominated by Paleozoic-age crystalline bedrock and glacial debris, except for Triassic-age sedimentary rocks in the New Haven areae The four major rivers which drain Connecticut and flow into the Sound are the Thames, the Connecticut, the Quinnipiac, and the Housatonic. The coast along the western half of northern Long Island is also highly irregular and is characterized by 10 recessed narrow bays which extend south and terminate at the Harbor Hill Moraine (Fig. 1); the eastern half has steep and high bluffs composed of unconsolidated glacial sediment which comprise the Harbor Hill Moraine that extends the entire length of long Island. The moraine is continuous from the eastern end of Long Island at Orient Point to about Port Jefferson where it forms coastal bluffs with relief in excess of 100 meters that are directly exposed to wave erosion. West of Port Jefferson the Harbor Hill Moraine joins with the Ronkonkoma Moraine and both extend westward as a broken line of hills toward Staten Island and northern New Jersey. 5e General Stratigraphy of Long Island and Connecticut. Detailed descriptions of the geologic units comprising Long Island are provided in Williams (1976); the units are summarized below and in Table l. Figure 3 shows that Paleozoic-age crystalline bedrock underlies Long Island at depths to several hundred meters and rises toward Connecticut. Upper Cretaceous-age semiconsolidated sedimentary strata that overlie the bedrock surface are thin to the north but thicken southward under the Sound and under- lie the Long Island mainland. The Lloyd, Raritan, and Magothy units consist of both marine and nonmarine sands and sandy clays and are important as fresh- water aquifers on Long Island. Tertiary-age rocks are known to be present under the Continental Shelf south of Long Island but are absent on the island, probably as a result of uplift and extensive erosion in Tertiary time. 13 eApnqs oy UT pesn $8109 Ai0jeIqTA pue seTtyroid UOTJSTFJet OTWSTes UOTINTOSeA ySTY oy OF suoyTzeoOT suTTYyIeAL *z eanSty ' hog SLOUIPAD) punog —_GNWISI Wd & punjsy yoo > Uodespug ONVISI SU3HSI ; 5 s \ a0) 9439 = alljo1g aIuisiag wy 02 Olegyzo Sn — al — 14 Table 1. Generalized stratigraphy of Long Island (from Williams, 1976). Character and origin of deposits Quartzose sand, beach and dune deposits, and fine- grained lagoon sediments - Pleistocene | Harbor Hill Moraine | Ground and terminal moraine; stratified deposits Ronkonkoma Moraine | of sand and gravel, cobbles, and silt and clay Holocene Cenozoic liqeeeeasy Quaternary Grayish-green, silty clayey, glauconitic fine sand (marine) 20-foot clay Gardiners Clay Grayish-green, silty clay (marine) Fine to very coarse-sand and gravel; scattered beds of silt and clay (fluvial or glacial outwash) Jameco Gravel Mannetto Gravel Monmouth Group Quartzose sand interbedded with silt and clay Matawan Group Magothy Formation Mesozoic Cretaceous | Upper Cretaceous Silty, sand, brownish-gray clay with thin beds of sand and gravel Raritan Formation Raritan Clay Lloyd Sand Precambrian Crystalline Bedrock or Paleozoic Quartzose fine to coarse sand and gravel; inter- bedded clay and silty sand is common Undifferentiated, consolidated, metamorphic granite LONG ISLAND Long Island SOUTH NORTH A A ATLANTIC OCEAN RONKONKOMA HARBOR HILL 100 FIRE ISLAND MORAINE MORAINE, ONG ISLAND SOUND CONNECTICUT SEA LEVEL Se EN ty eR I be ee 2 GLACIAL DEPOSITS SEA LEVEL -100 —200 —300 (ft) METAMORPHIC BEDROCK VERTICAL EXAGGERATION X20 Figure 3. Geologic cross section from the south shore of Long Island at Fire Island north across Long Island Sound to the Connecticut mainland (modified from De Laguna, 1963). 15 Pleistocene-age till and outwash deposits from at least two glacial epi- sodes overlie the Cretaceous strata and are responsible for much of the present-day relief on Long Island. Early Pleistocene glacial advances are thought to be represented by the Mannetto and Jameco gravels which are buried in places by the Gardiners clay which is believed to result from estuarine sedimentation during Sangamon timee Wisconsin Glaciation is well represented by the Ronkonkoma and Harbor Hill (terminal) Moraines and associated outwash sand plains that extend south of the moraines across the Long Island Inner Continental Shelf. The two moraines extend the length of Long Island and form the two forks at the eastern end. The same bedrock surface that underlies long Island forms nearly the entire mainland of Connecticut (Table 2). The only exception is in the New Haven area where a thick Triassic basin about 11 kilometers wide is present. To the east the basin is in fault contact with granitic bedrock; to the west the sandstones overlap the bedrock. Sanders (1963) first suggested that the basin continues south under the Sound and western Long Island, and this idea has been supported by results of magnetic surveys by Grim, Drake, and Heirtzler (1970). The bedrock surface of Connecticut has been deeply scoured by numerous glacial episodes and many of the river valleys were greatly deep- ened and widened; the bedrock is veneered with glacial deposits generally less than 10 meters thick except for the buried river valleys where thicknesses vary from 35 meters at the Housatonic River mouth to 244 meters at the Quinnipiac River (Upson and Spencer, 1964; Haeni and Sanders, 1974). Table 2. General stratigraphy of Connecticut. Era Period Character and origin Cenozoic Quaternary | Holocene Estuarine and marine soft organic muds from fluvial and shelf sources; modern marsh peat along coast Pleistocene | Localized and discontinuous ground till, moraine segments, and stratified sand and gravel outwash deposits Mesozoic Triassic tinue under Long Island Sound toward the Long Island mainland Paleozoic and Metamorphic and igneous crystalline Precambrian basement rock Along the north shore of Long Island, Holocene and modern sediments con- sist primarily of sands eroded from glacial bluffs exposed to wave attack. Fine-grained organic silts and clays in association with tidal marsh peat deposits are common from sea level to mean high water (MHW) along both the Long Island and especially the Connecticut shores, and thick accumulations of gaseous soft muds are present in the deeper parts of the Sound. A basin of sandstone, siltstone, con- glomerates and basaltic dikes intersect the shore at New Haven, Conn.; may con- 6. Bathymetrye Detailed morphology of Long Island Sound is provided by NOS hydrographic charts and bathymetric maps at scales of 1:80,000 and 1:125,000, respectively. 16 The major bathymetric trends and features from the NOS maps with seven selected profile locations are shown in Figure 4; the cross-sectional pro- files across the Sound are illustrated in Figure 5. Based on bathymetry, the Sound is divided into five major basins separated by shoals that have considerable relief. The western basin (profile A in Fig. 5) is rather narrow and water depths to 27 meters are common in the center but greater depths are present in small depressionse The central part of the Sound is composed of three basins with Cable and Anchor Reef, Stratford Shoal, and Six Mile Reef acting as the bound- ing shoals. Depths in the central basins usually do not exceed 30 meters, but some holes on the Long Island side extend to -46 meters. The eastern basin (profiles F and G in Fige 5) has considerably more relief, and depths in the elongate troughs may exceed 91 meters, such as “The Race” in profile G. 7. Previous Geologic Investigations. Long Island Sound is probably one of the most studied areas in the United Statese Dana (1890) was one of the first to speculate that based on land sur- face morphology and depth contours the ancient “Sound River” flowed eastward toward Block Island Sound and was responsible for eroding the trough that became Long Island Sound when sea level rose to its present position. How- ever, Veatch (1906) judged that the Sound River flowed west rather than east and breached western Long Island to join the sea» Fuller's (1914) study of the glacial deposits on Long Island gave support to Dana's eastward-flow theory for the Sound River but he believed that the major erosion took place in late Tertiary or early Pleistocene time, and that much of the present morphology of the Sound was the result of glacial erosion and depositional processes during late Wisconsin timee Fleming's (1935) study of central Long Island and its glacial geology pointed out that the Ronkonkana and Harbor Hill Moraines are composed mostly of stratified ice contact or glaciofluvial sand and gravel rather than till deposited directly at the glacier terminus. Investigation of the Sound continued with studies of the surface deposits on Long Island and Connecticut; however, in the 1950's new geophysical equip- ment was developed that allowed researchers to survey the Sound and look at the subbottom to give a third dimension to its geologic character. Oliver and Drake (1951) were about the first to use seismic refraction data to show that a very uneven bedrock surface underlies the Sound and is covered with glacial- age unconsolidated sediments. They were unable to identify Cretaceous strata in the Sound that were known to form the core of the Long Island mainland. Ellis (1962), in a detailed study of the sediments and geologic history of the Norwalk Islands between Stamford and Bridgeport, Connecticut, stated that the island chain was underlain by bedrock but that glacial till from a termi- nal moraine younger than the Harbor Hill formed most of the islands' relief. Upson and Spencer (1964) used deep boring logs from bridge foundation projects to describe the subbottom configuration and fill sediments of the ancestral channels of the Housatonic, Quinnipiac, and Thames Rivers that dis- charge into Long Island Sound. They found that all the valleys were eroded by glacial processes to bedrock and subsequently nearly filled with a sequence of glacial till, outwash sand and gravel, and estuarine silt and clay. Sanders (1965) and Haeni and Sanders (1974) used well boring logs and continuous 17 -SSOIO UaAeS JU ‘0 7 pu fy) °G SANSTY UT peqerASNT[E eae seTTyoad T[euotjoes *soinjeey Teoys pue pueyT zofeu ayy B3utmoys punog pueTsy Suoy jo Aaqowckyeg Jeey soyouy % ajgeg\ See, ‘ve eS, ( ee y ny Pees HERON HENS /-s Ue|S| Wid LAY Sst ry BB a MOCZ a7 Sp >) ae — Ge 2D SWOYJeY Ul SINO}UOD % Ole 9 70 Spezvio SS °h ainsTy 18 A Al B B! Shippan Pt. Lloyd Pt. Calf Pasture Pt. Eatons Neck MSL MSL pe— 50 36 100 ran (ft) 150 cannes 200 ony 250 256 (0) 2 4 nmi 0 2 4 6 8 nmi Point No Point Stratford Shoal Port Jefferson MSL 50 (ft) 100 150 ooo 5 2 4 6 8 10 a mi j D D! Mansfield Pt. Herod Pt. MSL @ 50} 100 (#1) 150 MSL 50 100 (4t) 150 200 250 MSL 50 (#t) 100 150 Se. Orient Pt. Plum Is. The Race Fishers 8: MSL 50 100 150 00 (ft) 2 300 350 400 450 0 aie 4 6 8 (OMMMnya Figure 5. Cross-sectional profiles of the Long Island Sound sea floor. See Figure 4 for profile locations. 19 seismic profiles to map the bedrock configuration of the ancestrial Quinnipiac River valley that underlies New Haven Harbor to depths of -224 meters and is about 2 kilometers wide. It is the deepest of any of the river valleys enter- ing the Sound and apparently follows Triassic faults and projects southwest into the Sound. Sanders (1965) described one boring that showed the upper 35 meters of fill sediment is sand and gravel outwash with frequent occurrences of estuarine organic mud. Presence of varved lacustrine deposits in coastal areas adjacent to the Sound led several investigators (Antevs, 1928; Frankel and Thomas, 1966; Bertoni, Dowling, and Frankel, 19/77) to surmise that one or more large freshwater lakes occupied the Sound during the Pleistocene epoch. Upson and Spencer (1964) and Williams (1976) show that these deposits also fill many of the deeply eroded river channels that were connected to the Sound when sea level was below present levels. Akpati (1970; 1974) reported results of a study on the surfacial sediments and foraminiferal ecology of eastern Long Island Sound to Fishers Island Sounde He examined grain textural properties and mineral compositions at 53 sites, including 3 of the CERC cores included in this report. Donohue and Tucker (1970) reported on marine minerals in Connecticut waters based on a program of coring at 8-kilometer grid spacing and using low-power acoustic profiling and bottom photography. They were able to identify some deposits of sand and gravel and certain heavy mineral concentrations, but the results appear to be of limited value for resource evaluation. The Pleistocene and Holocene history of the western Long Island region was studied in detail by Newman (1966); he reported evidence that a large glacial lake occupied the Sound region before the last ice advance, and that the sea began filling the Sound subsequent to about 12,000 years before present (BeP.). In 1970, the New York Ocean Science Laboratory started a study in eastern Long Island Sound to determine residual drift patterns of the surface and bottom waters. A preliminary report by Hollman and Sandberg (1972) showed that the Sound was stratified with surface waterflow out of the Sound at an average speed of 6 centimeters per second, and bottom waterflow into the Sound at 1.2 centimeters per second. Grim, Drake, and Heirtzler (1970) summarized 10 years of seismic reflec- tion and magnetic survey work on the subbottom character of the Sound. They report that the Paleozoic bedrock and Cretaceous sedimentary rocks are highly dissected and irregular with relief on the order of scores of meters and that Pleistocene and Holocene sediments fill most of the relief surfaces to produce the present rather shallow and even bottom. In eastern parts of Long Island Sound where it connects with Block Island Sound, McMaster and Ashraf (1973a, 1973b), Coch (1974), and Williams (1976) identified deeply buried stream channels which are pre-Pleistocene but acted as conduits for glacial advances and melt-water streams. These studies are germane to this study because many of the channels originated in Connecticut and traversed the Sound, and the processes responsible for the subbottom geologic character are similar throughout the entire southern New England region. 20 Feldhausen and Ali (1975) performed multivariate analysis on grain-size data from 5/ sample sites in the central and western basins of the Sound and identified 5 distinguishable sedimentary facies. They then related the facies to environments of deposition and subsequent modification by wind- and tide- generated currents. A major conclusion was that the rivers entering the Sound at present contribute minor volumes of sediment. Bohlen (1975) reported results of a 2-year study to measure the suspended- sediment budget at ll sites in eastern Long Island Sound. In contrast to other studies which show the central and western basins to behave like an estuary, Bohlen found that the eastern basin is well mixed and dominated by wind stress, tidal currents, and river discharge. For about the past 5 years, a group of researchers at Yale University has been reporting on studies done primarily in the central and eastern basins. Gordon (1974) examined by quantitative means the settling processes and dispersion of dredge material dumped at the authorized dump ground off New Havene Gordon and Pilbeam (1975) established bottom current meters at 28 stations to measure current velocities and the relationship to transport of bottom sediment. Bokuniewicz, Gebert, and Gordon (1976) used high-resolution acoustic profiles and short cores to estimate the areas and volumes of the unconsolidated sediments in the entire Sound in an attempt to produce a total sediment budget. One conclusion was that the volume of estuarine muds in place greatly exceed volumes that could have been supplied by rivers over the past 8,000 years and they propose that the open shelf is a primary source. Bokuniewicz, Gordon, and Kastens (1977) presented results of a study on the morphology and migration of a field of large sand waves (up to 4 meters high) in eastern Long Island Sound. They reported that sand waves will not form if more than 10 percent mud or 12 percent coarse sand (or larger) \is present, and that most waves were asymmetric to suggest transport into the Sound predominates. Recent studies by Sirkin (1976), Flint and Gebert (1976), and Newman (1977) have shown that late Wisconsin Glaciation in the Long Island region has been very complex and that the moraines and outwash deposits are often superimposed. Also, there is clear evidence that glacial advances younger than the one that left the Harbor Hill Moraine on the north of long Island have occurred, and their discontinuous moraines are still present. II. GEOMORPHOLOGY AND SHALLOW SUBBOTTOM CHARACTER 1. Shallow Subbottom Structure and Stratigraphy. Examination of the 700 kilometers of acoustic profiles collected shows that four major horizons or reflection units are present in Long Island Sound within the depth and resolution range of the equipment, usually about 91 and 0.5 meter, respectively. These are: (a) the floor of the Sound or sediment- water interface; (b) the top of Pleistocene sediments which include subre- flectors from glacial till, sand and gravel outwash, and lacustrine fine- grained strata; (c) the glaciated surface of Cretaceous-age semiconsolidated sedimentary rocks; and (d) the deeply dissected and smoothed surface of pre- Cretaceous consolidated rocks consisting of Precambrian and Paleozic bedrock and possibly Triassic strata in the region between New Haven and Northport, Long Island. The findings in this report agree with much of the basic Dal information contained in Grim, Drake, and Heirtzler (1970) concerning the subbottom geologic character of the Sound, though use of the sparker profiles in conjunction with the cores has provided more detail in many areas. ae Sea-Floor Reflector. The reflective character of the sea floor is dependent on the type of sediment comprising the upper parts of the sediment column. The Sound is generally floored by sands and gravelly sand along the north shore of the Long Island mainland and adjacent to many of the islands, shoals, and reefs in the middle of the Sound, as well as toward the Connecticut shore where glacial till and outwash detritus were deposited and subsequently reworked by waves and currents. Modern muds composed of silt, clay, and organic matter cover much of the central Sound and along the Connecticut shores The following three types of areas shown on the seismic profiles are identified with the core information: (1) Type 1. The first type denotes a very soft bottom where the upper several meters are composed of sandy silt or mud with high con- tents of organic matter and gase Records in these areas are almost opaque with a marked absence of any subbottom reflectors. The soft bottom acts as a sponge to the acoustic signal, absorbs the energy and prevents any significant penetration to the deeper reflectors. (2) Type 2. The second type shows a high degree of stratification starting at the surface and continuing with depth and allows the best penetration to reveal the subbottom character. The cores show that these areas are usually medium- and coarse-grained sands deposited as deltas and outwash fans. Often the surface in these areas has sand waves and megaripples as the result of the sediment being actively transported primarily by tidal currents. (3) Type 3. The third reflector type is normally very dark or strong on the seismic records and the region beneath is very light, showing only faint subbottom reflectors. Because the bottom is so hard there are normally three or more multiple reflectors on the profiles. These areas are characteristic of regions where consoli- dated bedrock is very close to the surface, where compacted glacial till is present and there are parabolic reflectors in the water column suggesting presence of boulders on the surface, and where very compact and well-sorted fine sand makes up the sea floor. be Pleistocene Sediments. The reflectors and sedimentary deposits assigned to a Pleistocene age are by far the most abundant and the most complex of any in the study areae Most of the information identifying the various subreflectors is based on published geologic studies of the New York and Connecticut mainland and of Long Island where only Pleistocene deposits overlie the Paleozoic and Cretaceous bedrock. Although most of the Pleisto- cene deposits are depositional, there is evidence of erosional episodes where channels have been downcut or widened and deepened by glacial or fluvial erosion and areas have been subjected to subaerial erosion. The thickest Pleistocene sediments occur in the bedrock valleys and chan- nels where highly stratified and thinly bedded strata conform to the topog- raphy of the underlying bedrock (Fig. 6)- Where these sediments have been penetrated by deep borings or exposed in surface excavations, they are thinly 22 (Ayl90]9A 13,DM) 4 ul yydaq *spues [eToeTs pue sjuewtpes pourTeis—suTy petyTzesqs ATysty Aq pereAOod pue PeTTT}J sxdeFINS YyooAIpseq jJeTTeA-y3Ty pue AeTNZei7A~ 9sy BuTMoys 121 96 OL SU SI SqnoTID.0uUOD seo ph toro iMG 4 i ‘SpueTS] ATeMI0N OUI FJO VTTJoAd DTwstes TeotTdAT (te teed sr 44 ~ : Sis : ; ' “4 AG ft re & ¢ i °9 9in3Ty ) aul (sw 23 laminated silt and clay with partings of fine sand. Their appearance closely resembles varve sequences related to seasonal sedimentation under quiet, low- energy conditions (Fig. 7). The surface elevation of this unit, termed the Flushing Formation by Newman (1977), varies considerably from near sea level to about -40 meters; its thickness has been documented by Williams (1976) to be 137 meters in the Orient Point buried channel and could be as much as 240 meters in a deep valley that runs southwest into the Sound at New Haven Harbore The origin of the deposits is long-term lacustrine deposition related to glacial lake Flushing that occupied deeper parts of the Sound from 15,000 to about 13,500 years ago (Newman, 1977). This lake was created immediately after retreat of the Harbor Hill glacier from long Island and probably was formed by damming of channels in the Block Island Sound region by glacial fill. The exact lateral extent of these lake deposits is difficult to deter- mine but similar, and probably related deposits, are present in deep valleys on the western end of Long Island and in the valley just south of New Haven; similar strata have been reported in eastern Long Island Sound and even parts of Block Island Sound (Bertoni, Dowling, and Frankel, 1977). The acoustic profiles from this survey also show that most of the central parts of the Sound contain stratified sediments overlying bedrock. The remainder of the Pleistocene sediments directly overlie either the lacustrine beds or bedrock and consist of glacial till and stratified deltas and outwash fans (mostly composed of sand and gravel) that originated adjacent to the moraines or as deposits from the melt-water streams that drained from the glaciers. As an economic resource these deposits are by far the most important, and their extent and character are covered in detail in the next section. The late Wisconsin-age Harbor Hill Moraine is nearly continuous across the entire north shore of Long Island and has been studied by many researchers interested in Pleistocene glacial events. It apparently resulted from a gla- cier that covered the Sound and parts of New England to the north, but much of the moraine actually consists of kame and kettle deposits marked by a high degree of stratification. The seismic profiles off the north shore of Long Island show no evidence of actual till deposits present. The shoreface region to depths of -18 meters consists of lobate and coalescing fans and deltas made up of medium- and coarse-grained sands that are outwash from the Harbor Hill Moraine. A number of researchers have recognized evidence, in the form of short, discontinuous, low-relief moraines, that glaciers younger than the Harbor Hill advance have occupied the Connecticut mainland. Goldsmith (1960) identified the Ledyard Moraine about 13 kilometers north of the Sound near New London, and also showed the position of the Middletown Moraine about 32 kilometers north of the Sound in central Connecticut. He attributes these moraines to temporary halts in the retreat of the glacier that formed the Harbor Hill Moraine. More recently, Flint (1968) and Flint and Gebert (1976) described the form and composition of the Madison and Old Saybrook Moraines on the coast east of New Haven (and their seaward extensions) and the Lordship outwash head southeast of Bridgeport. Flint (1968) was never able to locate or identify the moraine that had formed the Lordship outwash head but he speculated that it was possibly a western extension of the Madison or Branford Moraines, and that the outwash 24 SAMPLE: OEPTH: Figure 7. 17 SAMPLE: 19 SAMPLE: 20 SAMPLE: 22 igo - 162 ft DEPTH: § 170-172 ft DEPTH: 178-180 ft DEPTH: 188-190 ft SAMPLE: 27 SAMPLE: 25 SAMPLE: 26 DEPTH: 228-230 ft DEPTH: 208-210 ft DEPTH: 218-220 ft Photos of apparent varve sediments retrieved in the Orient Point boring drilled into the Orient Point buried channel. These suggest a major glacial lake occupied the long Island and Block Island Sounds during Pleistocene time. Each pair of light dark lines represents a summer and winter episode of lacustrine deposition (from Woodward-Clyde-Sherard and Associates, 1965). 25 fan resulted from deltaic sedimentation by the Housatonic River as it flowed south through the moraine. The Lordship head has a maximum dimension of almost 16 kilometers and extends well into the Sound, and is one of the most promising areas for sand and gravel. Using acoustic profiling equipment, Flint and Gebert (1976) surveyed areas of the Sound online with the Madison and Old Saybrook Moraines and were able to differentiate between bedrock islands close to the Connecticut shore and seven shoals and islands composed of till which are the morainal extensions. Their conclusions are also sup- ported by this study. Figure 8 shows that Crooked Shoal, Branford Reef, and Townshend Ledge are seaward extensions of the Madison Moraine, and that Kimberley Reef, Falkner Island, Goose Island, and an unnamed shoal represent extensions of the Old Saybrook Moraine. CONNECTICUT ) Guilford Branford Bedrock Boundary Madison Moraine Old Saybrook Moraine Hi] Branford Moraine Figure 8. Map of coastal Connecticut from Branford to Hammonasset Point showing the location and alinement of several shoals and islands determined to be remnants of the Madison and Old Saybrook Moraines (modified from Flint and Gebert, 1976). In western long Island, Newman (1977) identified the Elmhurst Moraine immediately north of the Harbor Hill Moraine in Queens County, Long Island, as an irregular and curving line of kame deposits (Fig- 9)- Based on its north- east strike, Newman extended the moraine into the Sound where it continues northeast defined by the shoal contours of Execution Rocks and the elongate shape and position of the Norwalk Islands. Based on radiocarbon dating, Newman (1977) believes that the Elmhurst glacial advance occurred about 13,500 years BP. and was part of the Port Huron readvance that took place in the Great lakes region. The geologic events are summarized in Table 3. The profiles and cores collected in this study have been useful in iden- tifying additional glacial depositional features shown in Figure 10. About 7.2 kilometers south of the Old Saybrook Moraine, a moraine segment almost 9 26 punog pueTsy suoyT ut yjA0u s9ya 07 Seinjesy YyseMzno pue sjusuzes suTeIOU AeBuNOK AOJZ BoUepPTAS poos ST e194] Inq ‘pueTs, Bucy BuoTe puayxe SouTeION euoYUoYUCY pue TTT at0qieg e8e-ursuoostmM e4ey ONNOS ONV7SI I074 PudjST ssaysiy 0 ¢ JUIOg YNDUOW) tu PuDIST Wg 3 2 ; 00022 °(3X9] UT pessnosTp) Jseoo 4ynoTJoeUUOD 3yR BuOTe pue Ave IINOIIA 10 ft \ \\ Pud|SsT aS009 pud|sy a Jauy| D4 $894 SIN XIS O0ok2 ' @ VAUGHAN OE Oo q4i0OH8 + 49294 piojsubjg °6 eINn3Ty NAW USS. | + 4aN su0j03 2@ yaay 0e 499N auos\y Fa |00US Joyduy 8 a1go) SpuDIs - Tomy Fes PsOswOjS + PJOj;D4IS N N O 44J0dabpisg P40; IW s G ‘ 9 . 2 Ny y + 00 o€2 27 Table 3. Summary of Quaternary geologic events (dates from Newman, 1977). 12,300 to present | As sea level rose, Long Island Sound became a tidal estuary and deposition of organic muds and sandy silts occurred. Sources of these sediments were and continue to be coastal erosion of glacial deposits, rivers drain- ing glacial terrain, and sediment influx from Block Island Sound and the adjacent Continental Shelf. Short-term readvance or slowing of retreat of the glaciers that were part of the Port Huron stade. This led to deposition of the several discontinuous terminal moraine segments (Elmhurst, Madison, Old Saybrook, Six Mile, Ledyard, and Middletown) close to the Connecticut coast on Long Island Sound. 15,000 to 13,400 | Damming by the Ronkonkoma and Harbor Hill Moraines backed up freshwater and created Lake Flushing that covered much of Long Island and Block Island Sounds. Very fine grained silt and clay. were deposited as seasonal varves filling in and covering the high-relief bedrock surface and glacial deposits. 21,000 to 15,000 Late Wisconsin advance of the glacier resulted in depo- sition of the Harbor Hill Moraine consisting of till and stratified kame and outwash deposits. Existing river valleys were deepened and widened. 72°40" CAORNEN@ ES G 1 1 1 LL MORE A \ noms 5 Je, a Sst 60 Hammonasset Poirit i tong Sond SWZ ss = a Sea Plum ie Island , —- 41°10" Orient Point Contours in Feet ee O 1 2 3 4 5 km 72°40" Figure 10. Flint and Gebert (1976) have shown that the Old Saybrook Moraine is present along the Connecticut coast from Niantic Bay to Hammonasset Point and then extends southwest into the Sound. Results of this study reveal that Six Mile Reef is a moraine segment and Long Sand shoal originated as an outwash deposit that has been lengthened to the west by estuarine processese 28 kilometers long and 1.8 kilometers wide is clearly defined on the two track- line profiles by its irregular subbottom character and almost 22 meters of sea-floor relief. The segment, named Six Mile Reef on the charts, represents the most southerly advance of very late Wisconsin Glaciation following the Harbor Hill episode. Its proximity to the Old Saybrook Moraine probably represents a seaward extension of that moraine, but additional subbottom data are needed to verify this. In the western Sound, segments of the Elmhurst Moraine were identified on several seismic records as subtle, broad mounds covered by about 5 meters of modern sediments (Fig. 9). Position of the Elmhurst Moraine in Figure 9 is close to what Newman (1977) theorized; at Execution Rocks it is about 1.8 kilometers wide and strikes east-northeast parallel to the Connecticut shore in an irregular and lobate line. South of Stamford Harbor the moraine is marked by several prom- inent shoals and to the east it is perched on a bedrock high and comprises the Norwalk Islands. Its trend continues toward Bridgeport and is no doubt responsible for the Lordship outwash head southeast of Bridgeport (Fig. 9). Another submerged outwash head located south of the town of Milford very likely marks the terminus of the moraine west of New Haven Harbor. The Branford Moraine segment east of New Haven is probably a continuation of that outwash head, but the proximity of the Madison, Old Saybrook, and Six Mile Reef segments suggests the glacier front had several small-scale advances and retreats in eastern parts of the Sound. In addition to the actual moraine features found, a number of highly stratified and elongate shoals containing very coarse-grained sediments are present in the Sound which apparently owe their origins to glaciofluvial or ice-contact processese Acoustic profiles and core 7 at Cable and Anchor Reef (Fig. 11) show that about 10 meters of very coarse sand in the form of forset strata rests on a bedrock high which continues south toward Long Island and meets the shore at Eatons Neck. Its proximity to the moraine forming the Norwalk Islands suggests a relationship; however, its general north-south orientation is normal to any other glacial deposition feature. A similar condition exists for Stratford Shoal in the middle of the Sound south of Bridgeport (Fig. 11). The shoal is 5-4 kilometers long with a north-south axis, and the seismic profiles suggest that the presence of stratified till or outwash overtop a bedrock high. The exact origins of these anomolous north- south features are not definitely known, but their form, forset-type strati- fication, and coarse sand and gravel composition suggest that they are outwash deltas from the ancestral Housatonic and Naugatuck Rivers. Additional inves-— tigations are needed to better understand their origins. Long Sand Shoal off the mouth of the Connecticut River is another sea- floor feature that originated from very late Wisconsin glacial processes. Its east-west orientation, asymmetric profile, and high relief suggest a morainal origin, but acoustic lines over the shoal show a high degree of internal stratification with forset strata dipping south; bedrock beneath the shoal is very high but there is no evidence of till reflectors. Cores obtained from the shoal show a composition of clean and generally moderately sorted sand, which suggests that it was a delta-front or outwash head that has probably been narrowed and significantly increased in length by Holocene estuarine processes during the past 12,000 years. 29 10° Bridgeport Se] Glaciofluvic! Oulwash Heads eye Norwolk Moraine 4 G & Poesesessned Resesesoseso} Norwalk scesscesece S3o5e5 ANY @ SoS eS oS oF e 4 bsososoe4 Norwalk Eatons soy 0 Contours in Feet Stony Brook LONG ISLAND 20 10° 73°00" == =) 0 ' 23 4 Skm Figure ll. The Norwalk Islands of Connecticut are remnants of a late Wisconsin moraine extending discontinuously from Queens County, Long Island, northeast to the New Haven areae The Lordship and Milford outwash deltas associated with that moraine and the positive relief features at Cable and Anchor Reef, Eatons Neck, Stratford Shoal, and Crane Neck also appear to have a glacial origin. ce. Cretaceous and Paleozoic Bedrock. The acoustic reflector marking the top of the bedrock is the strongest and most continuous of any on the records (Fig. 12). Except in deep channel areas such as off New Haven, in central parts of the Sound, and along much of the north shore of Long Island, the bedrock is present on the records. However, it is difficult to differentiate Cretaceous strata from underlying Paleozoic rock because of limited resolution on some profiles and lack of penetration into the Cretaceous strata. The exact northern limits of the Cretaceous cuesta are difficult to determine, but they appear to be close to the north shore of Long Island in the east and strike west through the center of the Sound in the vicinity of Stratford Shoal and then underlie the northern neck areas of western Long Island. The surface character of the bedrock is of extremely high relief, and contour patterns are difficult and at times impossible to identify in certain areas because of the extent of massive downcutting and widening of then exist— ing channels by the glaciers and melt water. In the western Sound, several large channels are present on both the Connecticut and Long Island sides and all appear to deepen toward the center of the Sound. Williams (1976) described six channels with thalwegs reaching -6l1 to -145 meters that under- lie the recessed bays of northwestern long Island and apparently transect the 30 Time (ms) f¢@$ a ~ 2800 Ft scenes ae 5 powers . ey ee eo SRS Sl lowomtie ea Behe eae om Oo ee 46 OSS GP SSE SSD RS NO EN Gav ber CARN O° SS Ge Cy es = ds Gar CELE Poa NS ede NAN ny 80 Figure 12. Typical seismic profile of a glaciated bedrock channel filled with Pleistocene sediments. Bedrock to the right nearly crops out at the sea floor. Sil Depth in ft (water velocity ) island and continue south across the shelf to intersect the present Hudson shelf channel. However, the connections with channels in the Sound have apparently been obliterated by glacial erosion because contour patterns do not matche Also, the unusual channel depths and reverse gradients to the north are the result of massive glacial erosion as the terminus remained at the Harbor Hill Moraine. In central parts of the Sound the bedrock surface is generally well below the depth range of the sparker records; however, Grim, Drake, and Heirtzler (1970) show a well-developed, characteristic glaciated east-west valley paralleling the north shore of Long Island from Port Jefferson east to about 72°30' We The sparker profiles show several tributary channels which trend south, but it cannot be determined from existing data if the channels also transect long Island and continue south across the shelf to a possible intersect with the Block shelf channel. The deep valley from the ancestral Quinnipac River that trends southwest from New Haven Harbor with a thalweg of -224 meters has been described by Haeni and Sanders (1974); the seismic records from this study show that it continues past Milford and Bridgeport to the north of Stratford Shoal, then changes to a more southerly orientation west of Stratford Shoal and probably connects with the -213-meter valley (described by Grim, Drake, and Heirtzler, 1970) underlying the north shore of Long Island at Stony Brook near Crane Neck (Fig. 11). The valley's southward continuation is not clearly defined, but Williams (1976) theorized that it connects with a buried channel present on the shelf 5.4 kilometers seaward of Moriches Inlet. The valley was certainly a major drainage channel before Pleistocene time, and its depth and width in the Sound rival the Hudson River fjord and make it by far the largest buried channel extension of the present rivers in Connecticut. The last bedrock channel of major significance is the buried extension of the Connecticut River which trends southeast from the present mouth toward Orient Point on Long Island. Sparker profiles several kilometers seaward of the river mouth show that the channel has a broad and open base with a thalweg of -78 meters (which is remarkably shallow), suggesting that glacial scour was not as pervasive as in other parts of the Sound. The channel continues south under Orient Point where glacial erosion has produced thalwegs of -152 meters and the channel has been filled with Lake Flushing varve sediments (Fig. 7). 2. Surface and Subbottom Sediment Character and Distribution. The lithologic character of the sedimentary deposits in long Island Sound to the maximum core recovery depth of 5 meters was determined by both macro- scopic and microscopic examination of samples from the 80 cores shown in Figure 13. Information on areas where cores were not taken was derived from extrapolation of the core data, using the CERC acoustic profiles, and from literature sources. Based on these analyses the surface and subbottom sediments have been classified, primarily by grain-size texture using mean grain diameter and 32 (BEB) Type WZ -coarse to very coarse sand ond gravel (4 phi). Figure 14 shows that type I sediments are most abundant in the deeper parts of the Sound and along the Connecticut shore, except along parts of the coast where glacial sand and gravelly deposits are actively eroded by waves. Type I materials originate from rivers, primarily the Connecticut and Thames, that drain glaciated terrain to the north and have brought fine-grained sediment to the Sound for about the past 12,000 years. In addition to contributions of the rivers, Bokuniewicz, Gebert, and Gordon (1976) believe that significant amounts of fine-grained material are trans- ported from Continental Shelf areas south of Long Island and are carried into the Sound and distributed westward by flood tidal currents. Cores 11, 13, 30, 32, 37A, 39, 45, 47, 50, 52A, 57, 59, 62, 73, and 77 show fine-grained sedi- ment overlying sandy sediment, and patches of opaqueness on the acoustic profiles suggest that pockets of type I sediment with high gas content are common in deeper parts of the basins. 33 Table 4. Grain-size scales--soil classification (modified from U.S. Army, Corps of Engineers, Coastal Engineering Research Center, 1977). Unified Soils |astm! mm | Phi Wentworth Classification | Mesh | Size | Value} Classification ees ee BOULDER COBBLE : ee 0 oo COBBLE COARSE : a GRAVEL [a Sc FINE Gravew|~—[ OE PEBBLE GRAVEL very =e ee | coarse | 0 very fine 34 *punog pueTsT B3uo] ut sedAj JUuSwTpes Arewtad ANOJ oy} JO UOT INGTAISTp JUeWTpes eoezins sy dew 07 pesn oi1eM SaTTJOid oTUsTes pue se10D OYAD “HT eaNnsTy e e@ ONNOS & ONVIST 49078 + Ne XZ 4018 9% 20 (ira wuGpe2lo Hodebpiig 4X (1ud p=) puns aut; Asan 04 Adjo pud yyis- 1 adhy & (1ud 2 0) >) puds wnipew of euly Ayan — TT adhy (!ud 1042) puds ass009 0; wnipaw - m adky (1ud|>) 120016 pun puns ass009 Asan 0) 851009 - AT adhy GN3931 02 ,O€ 0b 0G od 35 (2) Sediment Type II. These materials are very fine to medium grain- size sands from 0.125 to 0.5 millimeter (3 to 1 phi) primarily composed of quartz, feldspar, and rock fragments. These sands are most abundant along the Long Island coast where glacial sand outwash fans and the Harbor Hill Moraine are exposed to wave action and littoral processes (Fig- 14). Type II sands are also associated with the shoals and reef areas such as Cable and Anchor, Stratford, Middle Ground, Six Mile, and parts of long Sand Shoal off the Connecticut River. In eastern parts of the Sound, sand waves with heights reaching 4.6 meters are present on the profiles. Bokuniewicz, Gordon, and Kastens (1977) studied the area and found that bed forms do not form where there is more than 10 percent mud or 12 percent coarse sand. (3) Sediment Type III. These are medium to coarse sands in the size range from 0.5 to 1.0 millimeter (1 to O phi) with a composition similar to type II sediments except for higher percentages of rock fragments. The sedi- ments are commonly associated with type II and IV sediments and are found along the shore and in patches adjacent to shoals where strong currents remove the finer sediments and leave the coarser sediments as lag deposits. (4) Sediment Type IV. Materials with type IV sediments are coarse and very coarse sands and gravels larger than 1 millimeter (0 phi) in diam- eter, and are generally very poorly sorted. Because of the limiting diameter of the core barrel used in obtaining samples, the very coarsest materials in the cobble and boulder range are not represented; however, Ellis (1962), Flint and Gebert (1976), and Newman (1977) point out that boulders with diameters up to several meters are present in some of the glacial moraines and adjacent outwash heads.e As with the other coarse-grained sediments, type IV materials are limited to nearshore and shoal areas where glacial deposits are exposed to wave attack or strong littoral or tidal currents. Figure 13 shows that cores 7A, 21, 38, 70, and 74 contain several meters of type IV sediments that crop out on the surface, but cores 36, 22, 37A, 78, 52A, and Alpine 1 also show muds and finer grained sands overlying the very coarse material. III. BEACH-FILL NEEDS AND RESOURCE POTENTIAL 1. Sandfill Requirements for Long Island and Connecticut Beaches. The shoreline along the Atlantic coast from New Jersey to Cape Cod is probably the most heavily attended recreational area in the United States. The New York metropolitan area alone has more than 12 million people, and although most visit the Long Island south shore beaches there are a number of town beaches and public parks on the north shore that support recreation and periodically experience erosion problems where beach fill might provide a solution. Connecticut has numerous resort communities along the coast, particularly between the New York-Connecticut border and New Haven, with parks and beach areas that experience frequent erosion and storm flooding. In the past 40 years many of these beach areas have had some form of coastal engineering work; the 15 areas shown in Figure 15 have or may in the future involve beach nourishment. Sherwood Park, and the coastal segment from Silver Beach to Cedar Beach south of Milford, are the regions most likely to require renour- ishment in the near future. 36 38 . s(s = \s | ?. : Hartford ~ a | @ ro) 1B) | | E 9C en G.olN N Woterbury Norwich @ e 2 ° Om Meriden § $ C4 = 2242, New S LS e 2. New London @| s es Weta aa e @ ae \ Bridgeport Hammonosset Beach "Fairfield Se ty Guilford Point Beach : Norwalk P creninen rospect Beach * Woodmont Beach Gulf Beach Creenaich Point Silver Beach to Cedar Beach Cummings Park ‘Short Beach Beach Sasco Hill Beach Cove Island Beach Burial Hill Beach Colf Pasture Beach Sherwood Island State Park Compo Beach Figure 15. Projects along the Connecticut shore involving beach fill. All projects but Sherwood Park and Silver Beach to Cedar Beach are completed but may require future beach nourishment. 2. Suitability of Sand for Beach Nourishment. Sand should meet certain important criteria for use as borrow material in beach restoration and protection projects. Factors to consider are the (a) population mean grain size and total size distribution, (b) mineralogic com- position, (c) economics of sand recovery, and (d) placement and distribution on the beach. The borrow material should be of at least the same size and, preferably, slightly coarser than native material on the beach to be nour- ished. If borrow material was significantly smaller in particle size than indigenous sand it would be expected to be less stable and out of equilibrium with the wave and current regime. Consequently, it would be rapidly eroded and either carried offshore by wave-induced currents or transported parallel to the beach by longshore currents. In either case the net effect is acceler- ated retreat of the fill to readjust nearshore profiles, thus requiring con- siderably larger total volumes of initial fill and more frequent periodic replenishment. If the borrow sand does not have the same grain-size charac teristics as the native beach sand, the grain-size population of the borrow sand should preferably be more poorly sorted; i.e., a greater variation in size classes than the native beach sand, and initial overfill relative to the required volume of fill for sand with the same characteristics as that of the native beach would be necessary for comparable performance. Borrow material should be composed of hard, chemically and physically resistant minerals, such as quartz, which will not readily degrade in ‘the high-energy nearshore-beach-dune environmente Shi The subject of beach fill and its design is covered in detail by Krumbein and James (1965), James (1974), Hobson (1977), and U.S. Army, Corps of Engi- neers, Coastal Engineering Research Center (1977). 3. Primary Sand and Gravel Deposits. The seismic profiles and cores taken during this study reveal that 14 primary areas are present in Long Island Sound which contain relatively large quantities of sand and gravel that are accessible by conventional dredging methods. All areas in relation to the entire Sound are shown in Figure 16; the pertinent information for each deposit is included in Table 5. LiLiry) 012345 ani Liijiy 02468 10km Fishers Plum Island Gan clon a not BLOCK ISLAND Figure 16. The 14 primary sand and gravel deposits identified in Long Island Sound. The areal extent of each site is based on seismic data and bathymetric information; the thickness of each deposit was judged from the recovered sediment in the cores for each areas In many cases the seismic profiles show that sand in the deposits is considerably thicker than the amounts recovered in the cores, and that sand is also present in other parts of the Sound; however, the sand is either covered by various thicknesses of overburdens of modern fine-grained estuarine sediments, or is in water depths presently too deep for economic recovery. Therefore, a total volume of 189 million cubic meters of sand and gravel calculated for the entire Sound may be considered a conservative estimate and may be increased if additional long cores were used to explore the deposits in greater detail. ae Area A —- Matinicock Point Shoals. Area A consists of two irregular shoals inshore of the 15-meter depth contour to the northwest of Matinicock 38 Table 5. Characteristics of sand and gravel deposits. Designation Water depths | Thickness| Mean grain size Est. volume Remarke (m) (m) (mm) (million ow) 2.7 Deposit consists of two irregular ridges off Matinicock Point 8 to 18 0.60 to 0.90 Shoal about 6.4 km S. of Stamford is glacial till on a bedrock high Cable and Anchor Reef S. of Norwalk Islands is glacioflu- vial sediment on a bedrock high (yt 788 ie ce va a Shoal about 5 km SE. of Norwalk Islands consists of steeply dipping forset strata Shoal off Bridgeport is a glacio- fluvial delta with steeply SS forset strata Shoal off Crane Neck is composed of Pleistocene sands Deposit consists of glaciofluvial sands Shoal S. of Milford overlies the buried ancestral Quinnipiac River channel Shoal is well stratified with forset strata Townshend Ledge is composed of glaciofluvial sediment on a bedrock high 0.43 to 0. 48 0.40 to 0.65 0.34 to 0.79 0.43 to 0.84 Point on the Long Island north shore (Fig. 1/7). The reduction of seismic line 1 shown in Figure 18 shows the morphology of the shoals and the undulatory character of the bedrock as well as the position of core 31 taken on top of the nearshore shoal. Core 31 contains almost entirely medium grain-size quartz sande The character of the seismic profiles suggests that the shoals are composed of sandy material and probably have a similar origin. Using a sand thickness of 2./ meters, the calculated sand volumes for the nearshore shoal and the offshore shoal are 642 and 36/7 thousand cubic meters, respec- tively. These volumes may be quite conservative as seismic line 1 (Fig. 18) shows that the nearshore shoal is a maximum of 6 meters thick, and that the offshore shoal is about 4.6 meters thick. Shoal consists of Pleistocene glaciofluvial sands; sand waves with 5-m relief are present Long Sand Shoal is composed of stratified glaciofluvial and estuarine gands every Zn8 bedrock 'Data unknown. be Area B. Area B is an isolated shoal (Fig. 17) situated immediately south of Stamford Harbor and to the west of a designated dumping ground for dredge material. The shoal rises to within 7.9 meters of the water surface but its base lies in water depths of about 21 meters on three sides and slightly more than 30.5 meters to the northe The seismic data suggest that the shoal is composed of sedimentary material perched on a bedrock high; core 39 DTustes JusuTJIed |9Yy} JO suOoTIeDOT pue sjTsodep inoz B3uTMOYS puNog pueTS] Suc] uzazsem Jo dey °(399J UT SinojUOd) ejep 2109 pue */T 9ansta 10 * 906 p cr $ QNV1SI 9NO7 ion iy u, sunoquo9 WYbp ¢€ byt tt] $41SOdaq J8ADI9 puD puns QD wu 2 0 Cy 8/1j01g I1WS19Sg —»— a11$ 840) @ QN3937_ \ ‘ pasy dwng INDI LOANNOD ~ 3 BA a 40 NE Area ‘A’ Shoals : sw Matinicock Pt. Bottom Bottom no oes Oe cost SC OBIE HOTT a er ROT | Figure 18. Interpreted profile of seismic line 1 of two shoals off Matinicock Point (see Fig. 1/7 for location). 36, taken on the shoal in 14.3 meters of water, contains 0.9 meter of silty medium and coarse sand overlying 3.4 meters of poorly sorted, very coarse sand and gravel. These data support the calculation that 6 million cubic meters of sand and gravel is available for area B. The disadvantages of this site are its distance of more than 7 kilometers from the Connecticut shore in the middle of the Sound, and its proximity to the dredged-material disposal area. ce Area C —- Cable and Anchor Reef. This area is the largest of several shoal features which trend in a north-south line from the Norwalk shore of Connecticut to Eatons Neck Point on Long Island (Fige 17). Cable and Anchor Reef is in the middle of Long Island Sound surrounded by water depths of 21 to 34 meters, but it rises to within 6.7 meters of the water surfacee Seismic profile line 108 shows the shoal is composed of steeply dipping forset-type sedimentary strata; core 7A taken in 17./ meters of water in the northern end contains 3.1 meters of medium to coarse sand and gravel. Using a conservative thickness of 3.1 meters, the calculated sediment volume is 4 million cubic meters. The disadvantages of using this site for extraction of sand and gravel are the same as for area B to the west, except that two designated dredged- material disposal areas are immediately west of area C and any dredging activity would have to be coordinated with uses of the disposal areas. d. Area D - Eatons Neck Shoal. This site is part of a ridge extending north from Eatons Neck, Long Island, and apparently has a common origin with Cable and Anchor Reef (area C) to the north (Fig. 17). Both of these features probably relate to glaciofluvial depositional processes during the Pleistocene epoch. Area D is confined to water depths of 6 to 18 meters for practical purposes but its boundaries probably extend to the north at the apex of the -18-meter contour (Fig. 17). Seismic profile lines 5 and 6 show that the shoal is composed of forset-type strata; cores 26, 26B, and 38 show a compo- sition of fine to medium sand on the east and medium and coarse sand and gravel in the west. These data were used to compute a volume of 7 million cubic meters for available sand and gravel within area D. ee Area Ee Area E is located almost 5.4 kilometers southeast of the Norwalk Islands and 9 kilometers south of Sherwood Point, and is bisected by the 18-meter depth contour (Fig. 19). As shown in Figure 20, the area is on the distal end of a southward-projecting ridge characterized by high-angle forset strata. The ridge has an average thickness of 6 meters and appears to be closely underlain by bedrock. Core 9 was taken on the northern part of the 4l S n *e0Ys 4JNOFAIeuUCD 9|Yy, SuoTe q pue y satsodep Aazewtad jo dey N uy ° 4y ul SuNOyUO) $}1S0daq jaA019 pud puos | a]!yO1g I1WS1aS —.— Ob 811 8400 ® QN3931 O92!» oie! (i fe 140dabpiig h SIAIY J1V0J0SNOK LLNS I L GNNIOS OGNVIST INOT °61 Pansty 2° MJOMJON : JINNOOD 0; e ~N uy °o N nn 42 7 *SPUPTST ATEMION OY JO YSeoyAnos y vere BSUTSSOID COT-gq SUTT STWSTES jo eTTyoid pejzeadasquy °07 ein3Ty * ab tite stirs ei 35 Ht eBoy ae ants mS eee Sey = 4 z eno ' * . s ry ¥ = ” + Roe ed pee dat fem Fach deposit and contains 1.2 meters of medium to coarse sand overlying 2.7 meters of clean, coarse sand and gravel with 0.6 meter of fine to medium sand at the base of the core. The volume of sand and gravel within the limits of area E is calculated to be 4 million cubic meters; however, cores 42 and 44 suggest that the deposit may be considerably larger and may extend to the north and easte Cores 8 and 43 to the west contain sediment that is considerably finer in grain size than core 9 and both have a higher silt and clay content. f. Area F - Bridgeport Shoal. Area F is a triangular-shaped shoal about 7.2 kilometers southeast of Bridgeport at the mouth of the Housatonic River with its base at Lordship on the Connecticut shore, and its apex projecting southward about 5.4 kilometers into long Island Sound (Fig. 19). The shoal appears to end abruptly at the 18.3-meter contour but a discontinuous exten- Sion may continue south at Stratford Shoal toward Crane Neck on Long Island. Water depths over the deposit range from about 6 to 18 meters. Data coverage consists of two east-west and one north-south seismic profiles as well as cores 12 to 15, 49, 53, and 54. These data show that the shoal is a highly . Stratified outwash delta that varies in thickness from 0 to 9.1 meters, with the southern one-third being the thickest (Fige 21). This shoal appears to be the submerged and southerly extension of the Lordship outwash head described by Flint (1968). On land the outwash feature is composed of coarse-grained sediment with boulders as large as 1 meter. This sediment may also be present in area F, but none is obvious from the seismic data. The sand body probably originated as a glaciofluvial delta of the Housatonic River during a very late Wisconsin glacial advance in central Connecticut. All seven cores in this area contain sand and only core 54 penetrated the sand body and recovered an underlying substratum of dark brown clay. Cores 1/7 and 48 to the west and cores 50, 51, and 52A to the east of the deposit show the shoal flanks are overlapped by muddy modern sediments which blanket adja- cent bottom areas. The sand contained in the outwash shoal is typically light brown, medium to coarse (0.25 to 1.00 millimeter; 2.0 to 0.0 phi) quartz sand with sparse shells and, locally, up to 15 percent small gravele Since the sand is clean, generally free of fine particles, and is sufficiently variable in size charac-— teristics from place to place, selective borrowing could be used to obtain desired size grading. Computations based on the seismic and core data show that the Bridgeport area has the highest potential of any of the deposits along the Connecticut shore of Long Island Sound. Using a thickness of 3.9 meters, the sand and gravel volume is 37 million cubic meters; however, the actual inplace volume may be more than twice this amount. ge Area G. Area G, a circular deposit north of Old Field Point and Crane Neck on the Long Island northshore (Fige 22), lies within the 6- to 15-meter contours and is defined by seismic profile line 11 and core 2l. The seismic profile shows the area is underlain by horizontal sedimentary strata and core 21 contains a fairly uniform mixture of silty fine to very coarse sand with pebbles up to 6.4 centimeters in diameter. The deposit appears to have origi- nated from Pleistocene glaciofluvial or glacial deposition processes and may be genetically related to the Bridgeport deposit (area F) and Stratford Shoal, both of which are alined to the north across the Sound. The limited data cov—- erage in area G makes resource calculations inprecise but based on a thickness of 3.3 meters, the computed volume of sand present. is 5 million cubic meters. 44 euOTIeBOTJTIeAIS JesiroF BuTMOYsS (q e21e) peey ysemjzno dtTyspi0oy ey} Jo pues yyNos 9yI 3e ZZ-gq SUTT jo eTTyoId peqeadiajuy *1Z eansTy 45 20 15 + + LONG -ISLAND SOUND +40°55° North Port LONG ISLAND LEGEND © Core Site —32_ Seismic Profile @@ Sana ana Gravel Degosits Contours in ft 10° 73°05 Figure 22. Map of sand and gravel deposits D and G along the north shore of Long Island. j he Area H — Port Jefferson Shoal. The Port Jefferson deposit is on the north shore of Long Island 3.6 kilometers east of area Ge Area H lies in water depths of 6 to 15 meters and, like area G, is defined by one seismic profile and core 78 (Fig.e 23). Core 78 shows that the top 0.5 meter of the deposit consists of silty medium sand underlain by coarse sand to -1.8 meter, and that the base of the deposit to -2.-/ meters is composed of brown, poorly sorted fine to very coarse sand and significant amounts of pebbles. The area H deposit is closely related to the adjacent Harbor Hill Moraine, and is pos-— sibly continuous with area G to the west as well as with areas J, L, and M to the east. Offshore, the sand and gravel of area H is overlapped by fine- grained sediments. The calculated volume of sand and gravel in the area is 5 million cubic meters based on a thickness of 2-/ meters. ie Area I - Milford Shoal. Area I is situated about 1.8 kilometers off the Connecticut coast just south of the town of Milford and southwest of New Haven (Fig. 24). It comprises the southern part of a shoal which extends from about the -—6-meter water depth close to shore to the -9-meter contour 2./ kil- ometers offshore. Core 5/7 at the northern part of the shoal shows that it is composed of fine to very coarse sande The periphery of the shoal is sharply defined and cores 55 and 56 to the southwest and northwest show the adjacent bottom is considerably finer in grain-size diameter. Using a thickness of 3./ meters, the computed volume of sand and gravel in area I is 10 million cubic meters. . 46 55° 50° LONG ISLAND SOUND TIS LINE 28 c =; “ = WY = oT RO. 2 229. LINE 14 “Port Jefferson LONG ISLAND oF ee EGEND te cnoss © Core Site —3°_ Seismic Profile @® Sand ona Gravel Deposits Contours in ft 72°40° Figure 23. Map of the Long Island north shore from Port Jefferson to Roanoke Point showing potential borrow areas H, J, and L. 4105, . 0 ae Cr n CONNECTICUT New Haven Falkner Island if oC” eer eee ee ——— ie ee LEGEND “i LONG I[SLANO SOUND © Core Site —32_ Seismic Profile @BD Sond and Gravel Deposits : 10" Contours in ft oO Ss rv °o ww Ly Figure 24. Map of deposits I and K near New Haven, Connecticut. Area I is the Milford outwash head and Townshend Ledge is a moraine remnant. 47 je Area J. Area J, approximately 9 kilometers east of area H and imme- diately offshore of North Shore Beach, is defined by seismic lines 16 and 28 and core /76,. and consists of an outwash shoal from the Harbor Hill Moraine. The surface of the shoal is characterized by several northeast-oriented ridges (Fig. 23) with relief up to 6 meters; seismic line 16 shows that the shoal is highly stratified with forset strata. Core 76 on the nearshore part of the deposit is composed of 1./ meters of silty medium sand overlying 1.8 meters of medium to very coarse sand and small pebbles. The calculated sand volume within area J is 7 million cubic meters. ke Area K - Townshend Ledge. This area is located about 2./ kilometers south of the Connecticut coast and just east of the entrance navigation chan- nel to New Haven (Fig. 24). Area K rises to within 5.5 meters of the water surface; the base is in about 10.4 meters of water to the north and up to 15.2 meters to the southe It is bisected by seismic profile 115, and core 538A was taken in -11.3 meters of water toward the western end. The seismic profile shows bedrock to be fairly high in the area but the ledge itself exhibits internal stratification. Core 58A shows that the strata consist of silty medium sand for the upper 0.5 meter and clean medium to coarse sand for the next 1./ meter. Based on these data, the estimated volume of sand is 3 million cubic meters; however, this volume could actually be several times larger if the total relief for the entire ledge were considered. Core 59 to the south of area K shows that gray, fine-grained modern sed- iment blankets the adjacent bottom and covers large quantities of sand and gravel that are probably contiguous with the sediments on Townshend Ledge. Core 59 shows 0.9 meter of silt overlying 1.7 meters of brown, clean, medium to coarse sand. 1. Area L — Roanoke Point Shoal. Area L is about 8 kilometers east from area J along the north shore of Long Island between the major headland shoals at Herod Point and Roanoke Point (Fig. 23). The area comprises the shoreface region beween the -6- and -18-meter contour and is transected by three seismic profiles; however, core 75 provides the only information on the actual physi- cal character of the sediments in the deposit. Like the other deposits along the north shore of Long Island, area L is an outwash plain from the Harbor Hill Moraine to the south, but the presence of large bed forms on the bottom suggests that the surficial sediments are being actively modified by present— day estuarine tidal currents. Core 75 was taken on the nearshore part of the deposit in 7 meters of water and contains 3.9 meters of fairly homogeneous, clean, fine to medium sand. The seismic profiles show that these sandy sediments are probably contiguous through the entire deposit. Seismic profile 28 offshore of the deposit shows that older fine-grained sediments are present from fixes 738 to 752, which probably represent glacial Lake Flushing lacustrine deposits. Based on core 75, a sand thickness of 3.8 meters was extrapolated over the area to compute a total sand volume of 40 million cubic meters. me Area Me Area M, an elongate deposit more than 10.8 kilometers long and about 1.8 kilometers wide north of the town of Mattituck (Fig. 25), occu- pies the shoreface between the -3- and -18-meter contours; the presence of sand waves with relief up to 4-6 meters shows that the area is frequently 48 LONG ISLAND Mattituck x “Shelter ihand - LEGEND © Core Site 6 73° _ Seismic Profile . @2B Sond ana Gravel Deposits “og. Contours in ft 2 Figure 25. Map of borrow area M along the Long Island north shore. subject to strong tidal surges. Seismic line 29 shows internal stratification in the deposit; core 74 to the west and core 72 on the eastern end contain 4 and 2.3 meters of clean, fine to coarse sand and pebbles, respectively. Seismic lines 21 and 22 show that the sand thins abruptly offshore and that flat-lying, fine-grained strata are present at -19.5 meters. Using a thick- ness of 2.7 meters, the deposit contains an estimated 54 million cubic meters of sand and gravel. The seismic data and core 70 to the east of area M show that stratified sandy sediments continue well beyond the boundaries of area M; however, the -18-meter contour is very close to shore, hence the deposits are probably confined to a narrow band and removal of large quantities could adversely affect stability of the adjacent coast. ne Area N —- long Sand Shoale Long Sand Shoal, an elongate, slightly arcuate ridge about 3.5 kilometers off the mouth of the Connecticut River has a total length of 10.8 kilometers and a maximum width of less than about 450 meters, and tapers to the east and west. The minimum water depth over the shoal is 2.4 meters and the adjacent bottom to the north is on the order of 12.2 meters; the bottom drops abruptly to the south to depths of 45.7 meters within 1.8 kilometers of the shoal (Fig. 26). There are several seismic profiles that run up to and adjacent to the shoal, but the extreme shallow water prevented the survey vessel from crossing the shoal. In addition, cores 64, 65, 66, and 67A taken on the shoal flanks provide good physical evidence of the subbottom character of the shoal. 49 s 72°25" 20° ; 15° nari CONNECTICUT * Connecticut River ‘Miontic River 15° 200,520 i : a s noal 5 Fishers Island Long Sond e & Ee Great Gull © Plum Island BLOCK ISLAND 4ie10" + +41°10' SOUND LEGEND © Core Site G —2_ Seismic Profile e @ Sana ona Grovel Deposits Contours in ft 72°25° 0s" - 72° CONNECTICUT Guilford 20 41°15' + 225 Long Sand Shoal c sree 9 eee Falkner Island So , Six a Reef pi LONG ISLAND SOUND Melia 41°10" + + + 41°10' LEGEND ® Core Site 73° Seismic Profile @B Sand_and Grovel Deposits Contours in ft 72°25 Figure 26. Map of eastern Long Island Sound showing the morphology of Long Sand Shoal. 50 Figure 27 shows that the bedrock surface in the vicinity of Long Sand Shoal is undulatory and has been deeply scoured by Pleistocene glaciers. The irregular bedrock surface has been filled and covered by flat-lying sedimen- tary strata which in turn are overlain by the almost horizontal strata com- prising the shoale Apparently, bedrock is about 11 meters beneath the shoal at fix 214; cores 66 and 6/7A show that the strata on top (which make up the shoal) are fairly uniform, fine and medium grain-size sands with thicknesses of 3.2 and 4./ meters, respectively. Core 68, taken on the southern flank in 31 meters of water, shows that the sand pinches out and overlies older fine- grained sediments which probably are the horizontal strata filling the bedrock depressions shown in Figure 27. Cores 64 and 65 to the north of the shoal contain silty, very fine and fine-grained sediments which would be unsuitable for fill material. , Horizontal Scale CERC LINE IZia (0) 100 (m) Navigation Fixes 214 208-— 204 Water Long Sand Shoal Surface Fluvial Outwash Sediments Sea floor See 56 Fine-grained 4 m Lacustrine Sediments Figure 27. Interpreted profile of seismic line 12la over Long Sand Shoal. The Bedrock surface closely underlies the shoal which is charac- terized by highly stratified sandy sediments covering both bedrock and channel-filling fine-grained sediments. Based on the limited seismic and core data available, Long Sand Shoal probably contains enough suitable sand to be designated a high potential deposit. Most of the largest grain-size sand is apparently concentrated along the main axis of the shoal or on the southern flank; the sediments on the northern flank are finer grained and have higher percentages of silt and clay. Using a thickness of 2./ meters over the area shoaler than the -6-meter con- tour yields a total sand volume of 6 million cubic meters. Although Long Sand Shoal offers potential as a deposit, more densely spaced sediment samples are needed to reliably define its potential. IVe SUMMARY A detailed geological study was made of long Island Sound using high- resolution seismic reflection profiles and long sedimentary cores to decipher the Quaternary geologic stratigraphy of the Sound and, in particular, to assess the sand and gravel resources. Results from the study show that the deepest acoustic reflector is the bedrock surface which crops out on the Connecticut mainland and slopes south to depths of -250 meters at the north shore of Long Island. Bedrock is over- lain in isolated areas by Cretaceous strata which have been deeply scoured by multiple glacial advances and long episodes of fluvial erosion. Pleistocene sediments are ubiquitous as thick accumulations of firm lacustrine silt and 51 clay, as well as silty sands and gravels that were placed as discontinuous recessional moraine segments and outwash fans. Holocene sediments consist primarily of organic sandy muds that are accumulating in low-energy areas where tidal currents and wave action are minimal. Fourteen shoal areas distributed around the Sound were found to offer the highest potential as sources of sand and gravel. Based on the seismic data and core results, these resources are conservatively calculated to be 189 million cubic meters in water depths less than 20 meters. 52. LITERATURE CITED AKPATI, B.Ne, “Mineral Composition and Sediments in Eastern Long Island Sound, N.Y.," Maritime Sediments, Vole 10, Noe 1, Apr. 1974, pp. 19-30. AKPATI, BeNe, “Sedimentation and Foraminiferal Ecology in Eastern Long Island Sound, New York,” Ph.D. Dissertation, University of Pittsburgh, Pittsburgh, Pae, 1970. ALPINE GEOPHYSICAL ASSOCIATES, INC., “Sparker, Echo Sounder and Vibracoring Geophysical Site Investigation: Proposed Bridge Eastern Long Island Sound,” Final Report, Oct. 1965. AMERICAN ASSOCIATION OF PETROLEUM GEOLOGISTS, “Seismic Stratigraphy - Application .to Hydrocarbon Exploration,” C.E. Payton, ede, Memoir 26, Tulsa, Okla., 1977. ANTEVS, E., “The last Glaciation," American Geographic Society, Research Series 17, 1928. BERTONI, Re, DOWLING, J., and FRANKEL, Le, “Freshwater-Lake Sediments Beneath Block Island Sound,” Geology, Vole 5, Octe 1977, ppe 631-635. BOHLEN, W.eF., “An Investigation of Suspended Material Concentrations in Eastern Long Island Sound,” Journal of Geophysical Research, Vol. 80, No. 36, Dece 1975, ppe 5089-5100. BOKUNIEWICZ, H.J., GEBERT, J., and GORDON, R.B., “Sediment Mass Balance of a Large Estuary, Long Island Sound,” Estuarine and Coastal Marine Science, Vol. 4, 1976, pp. 523-536. BOKUNIEWICZ, HeJe, GORDON, R-Be, and KASTENS, KeA., “Form and Migration of Sand Waves in a Large Estuary, Long Island Sound,” Marine Geology, Vol. 24, US775 pps l85—199! COCH, Ne, “Morphology and Sediment Distribution in Deep Channels Connecting Long Island and Block Island Sounds, New York,” Memorial Institute of Geology, Bassin Aquitaine, No.- 7, France, 1974, pp. 241-246. DANA, J-D., “Long Island Sound in the Quaternary Era, with Observations on the Submarine Hudson River Channel," The American Journal of Scetence, 3d Series, Vole 60, Noe 240, Dec. 1890, pp. 426-437. DeLAGUNA, We, “Geology of Brookhaven National Laboratory and Vicinity, Suffolk County, New York,” Bulletin 1156-A, U.S. Geological Survey, Washington, D.C., 1963, PPe Al-A55. DONOHUE, JeJe, and TUCKER, F.Be, “Marine Mineral Identification Survey of Coastal Connecticut,” Final Report J-9/70660-1, United Aircraft Research Laboratories, United Aircraft Corporation, East Hartford, Conn., Jan. 1970. DUANE, D.B.-, et ale, “Linear Shoals on the Atlantic Inner Continental Shelf, Florida to Long Island," Shelf Sediment Transport, Dowden, Hutchinson, and Ross, Ince, Stroudsburg, Pae, 1972, ppe 447-498 (also Reprint 22-73, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Va.-, NTIS 770 172). 53 ELLIS, C.W.e, “Marine Sedimentary Environments in the Vicinity of Norwalk ‘Island, Connecticut," State Geological and Natural Htstory Survey of Connectteut, Bulletin No. 94, 1962. FELDHAUSEN, P.H., and ALI, S.A, “Sedimentary Environment Analysis of long Island Sound, USA with Multivariate Statistics,” I.M.G., Secession, IX Congress International de Sedimentologic, Nice, France, July 1975. FIELD, M.E., et al., “Upper Quaternary Peat Deposits on the Atlantic Shelf of the United States,” Bulletin of the Geological Soctety of America, Vol. 90, July 1979, pp- 618-628. FLEMING, WeLeS., “Glacial Geology of Central long Island,” American Journal of Setence, 5th Series, Vol. 30, No. 17, Sept. 1935, ppe 216-238. FLINT, R.F., “The Surficial Geology of the Ansonia and Milford Quadrangles,” Connecticut Geologic and Natural History Survey Quadrangle Report 23, Hartford, Conn., 1968. FLINT, R-F., and GEBERT, J-A., “latest laurentide Ice Sheet: New Evidence from Southern New England,” Bulletin of the Geological Soctety of Amertca, Vol. O7/ Febe 1976, PPpe 182-188. FRANKEL, Le, and THOMAS, H.F., “Evidence of Freshwater Lake Deposits in Block Island Sound,” Journal of Geology, Vole 74, 1966, ppe 240-242. FRIEDMAN, GeM., “On Sorting, Sorting Coefficients, and the Lognormality of the Grain Size Distribution of Sandstones," Journal of Geology, Vole 70, 1962, pp-e 737-756. FULLER, M.L.-, “Geology of Long Island, New York," Professional Paper 82, U.S. Geological Survey, Washington, D.C., 1914. GOLDSMITH, R-e, “A Post-Harbor Hill-Charleston Moraine in Southeastern Con- necticut,” American Journal of Setence, Vole 258, Dec. 1960, pp. 740-743. GORDON, R-B., “Dispersion of Dredge Spoil Dumped in Near-Shore Waters,” Estuarine and Coastal Marine Setence, Vole 2, 1974, ppe 349-358. GORDON, R-B., and PILBEAM, C.C., “Circulation in Central Long Island Sound,” Journal of Geophystcal Research, Vol. 80, Noe 3, Jane 1975, ppe 414-422. GRIM, M.S., DRAKE, C.L., and HEIRTZLER, JeR., "Subbottom Study of Long Island Sound,” Bulletin of the Geological Soctety of America, Vole 81, Mar. 1970, pp- 649-666. HAENI, F.P., and SANDERS, J-eE., “Contour Map of the Bedrock Surface, New Haven-Woodmont Quadrangles, Connecticut,” Miscellaneous Field Studies, Map MF-557A, U.S. Geological Survey, Washington, D.C., 1974. HALL, J-V.-, Jre, “Artificially Nourished and Constructed Beaches,” TM-29, U.S. Army, Corps of Engineers, Beach Erosion Board, Washington, D.C., Dec. 1952. 54 HOBSON, R-D., “Review of Design Elements for Beach-Fill Evaluation,” TP 77-6, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Vae, June 1977. HOBSON, RD., “Definition and Use of the Phi Grade Scale,” CETA 79-7, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Va-e, Nove 1979. HOLIMAN, R., and SANDBERG, G.Re, “The Residual Drift in Eastern long Island Sound and Block Island Sound,” Technical Report Noe 0015, New York Ocean Science laboratory, Montauk, N.Y., June 1972. JAMES, WeR., “Beach Fill Stability and Borrow Material Texture," Proceedings of the 14th International Conference on Coastal Engineering, American Society of Civil Engineers, 1974, ppe 1334-1347 (also Reprint 13-74, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Va., NTIS AO1O 753). KRUMBEIN, WeCe, and JAMES, WeRe, “A lognormal Size Distribution Model for Estimating Stability of Beach Fill Material,” TM-16, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Washington, D.C., Nove 1965. MAURIELLO, LeJe, “Experimental Use of Self-Unloading Hopper Dredge for Rehabilitation of an Ocean Beach," Proceedings of the First World Dredging Conference, World Dredging Association, Vol. 67, 1967, ppe 367-395. McCABE, ReA., “Beach Behavior, North Shore, Long Island Sound,” Journal of the Waterways, Harbors and Coastal Engineering Diviston, Vole 96, Noe WW4, Nov. 1970, pp. 781-794. McMASTER, ReLe, and ASHRAF, A., “Subbottom Basement Drainage System of Inner Continental Shelf off Southern New England,” Bulletin of the Geologtcal Soctety of America, Vol. 84, Jan.e 1973a, pp- 187-190. McMASTER, R-eL-e, and ASHRAF, A., “Extent and Formation of Deeply Buried Chan- nels on the Continental Shelf off Southern New England,” Journal of Geology, Vol. 81, 1973b, PpPpe 374-379. MOORE, D.G., and PAIMER, H.P., “Offshore Seismic Reflection Surveys,” Proceed- ings of Conference on Civil Engineering in the Oceans, American Society of Civil Engineers, 1967, pp. 789-806. NEWMAN, W-S., “Late Pleistocene Environments of the Western Long Island Area,” Ph.D. Dissertation, New York University, New York, N-Y., 1966. NEWMAN, W.S., “Late Quaternary Paleoenvironmental Reconstruction: Some Con- tradictions From Northwestern Long Island, New York," Annals of the New York Academy of Setences, Vol. 288, Feb. 1977, ppe 545-570. OLIVER, J-E.-, and DRAKE, C.L.-, “Geophysical Investigations in the Emerged and Submerged Atlantic Coastal Plain,” Bulletin of the Geological Society of America, Vole 62, Nove 1951, ppe 1287-1296. PILKEY, O.H., and FIELD, M.E., “Onshore Transportation of Continental Shelf Sediment: Atlantic Southeastern United States,“ Shelf Sediment Transport, Dowden, Hutchinson, and Ross, Ince, Stroudsburg, Pae, 19/72, pp. 429-446. 55 SANDERS, J-E., “Late Triassic History of Northeastern United States," American Journal of Setence, Vol. 261, 1963, pp.e 501-524. SANDERS, JeE., “Sediment-Filled Deep Valleys Underlying New Haven Harbor, Connecticut, Revealed by Continuous Seismic Profiling Using Sparker and Pneumatic Sources," Transactions of the American Geophysics Unton, Vol. 46, No. 1, 1965. SIRKIN, LeAe, “Block Island, Rhode Island: Evidence of Fluctuation of the Late Pleistocene Ice Margin,” GSA Bulletin, Vole 87, Apr. 1976, ppe 574-580. UPSON, J-eE., and SPENCER, C.W.e, “Bedrock Valleys of the New England Coast as Related to Fluctuations of Sea Level,” Professional Paper 454-M, U.S. Geologic Survey, Washington, D.C., 1964. U.S. ARMY, CORPS OF ENGINEERS, COASTAL ENGINEERING RESEARCH CENTER, Shore Protection Manual, 3d ede, Vols. I, Il, and III, Stock No. 008-022-00113-1, U.S.e Government Printing Office, Washington, DeC., 1977, 1,262 pp. VEATCH, A.C., “Outlines of the Geology of Long Island,” Professional Paper 44, Underground Resources of Long Island, U.S. Geologic Survey, Washington, D.C., 1906. WILLIAMS, S.J., “Geomorphology, Shallow Subbottom Structure, and Sediments of the Atlantic Inner Continental Shelf off Long Island, New York,” TR 76-2, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Vae, Mar. 1976. WILLIAMS, S.J., “Geologic Effects of Ocean Dumping on the New York Bight Inner Shelf," Ocean Dumping and Marine Pollutton, Dowden, Hutchinson, and Ross, Ineo, Secouclsiwmresy, wo, IW/Y, po Dile/Zo WILLIAMS, S.J.-, and DUANE, D.B., “Regional Shelf Studies--A Guide to Engi- neering Design,” Proceedings of the Eighth Annual Conference of the Marine Technology Soctety, 1972, ppe 227-236 (also Reprint 3-72, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Vae, NTIS 754 869). WILLIAMS, S.J., and DUANE, D.B-, “Geomorphology and Sediments of the Inner New York Bight Continental Shelf,” TM-45, U.S. Army, Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Vae, July 1974. WOODWARD, CLYDE, SHERARD, AND ASSOCIATES, “Boring Supervision and Laboratory Tests of Proposed Suspension Bridge, Orient Point, long Island," Clifton, NeJe, Oct. 1965. 56 APPENDIX A CORE SEDIMENT DESCRIPTIONS Appendix A contains visual descriptions of sediment from cores in the study areas Except where noted, sample locations are shown in Figure 2. Visual descriptions for the CERC cores are based on both megascopic and microscopic examination. Sediment color is based on dry sample per Munsell Soil Color Charts (Munsell Color Company, Inc., Baltimore, Maryland, 1954 Edition). Sediment names are based on the Wentworth size-scale as follows: Sediment Size (mm) Phi Gravel >2 <1 Very coarse sand 1.0 to 2.0 0 to -l Coarse sand 0-5 to 1.0 1 to 0- Medium sand 0-25 to 0.5 2towl— Fine sand 0.125 to 0.25 3 to 2- Very fine sand 0.0625 to 0.125 4 to 3- Silt and mud <0.0625 >4 Sorting terms! Phi rr Very well sorted 0.35 Well sorted 0.50 Moderately well sorted 0.80 Moderately sorted 1.40 Poorly sorted 2.00 Very poorly sorted ~ 2.60 Extremely poorly sorted a lverbal sorting terms from Friedman (1962). The contents of the core samples are tabulated in Table A-1. Table A-1. Description of Alpine cores shown in Figure 13.! Core Depth Description Noe (ft) North Orient Point (water depth 48 ft) Black mud Black silty sand Sand, medium grain, tan Gravel, tine-grained, mixed with about 10 pct sand Gravel, coarse 0./75- to 3-in pebbles Refusal East of Gull Light (water depth 44 ft) Black mud Sandy silt, beige color Silty sand, fine-grained, closely packed Refusal lFrom Alpine Geophysical Associates, Inc. (1965). 57 Table A-2 Sediment description from cores in Long Island Sound. Core No. | Water depth Internal Description mee ©) Nie CERI aR} 0 to 6.3 Gray (2.5Y Geay Chey GD) Rois eta, cites Gees moderately sorted, medium to course quartz sand 2A 56 0 to 2 Gray (5Y 6/1) medium sand, well sorted, with small pebbles 2 to 2.5 (5Y 6/2), fine to medium sand 2.5 to 4 (SY 6/2), poorly sorted, fine to coarse sand 4 Gray (5Y 7/1) silt 4 21 0 to 12.5 | Gray (5Y 7/2) silt 12.5 to 13.4 (5Y 8/2), clean medium to coarse sand 5 27 Ontor4e5 Gray (5Y 6/1) very fine sand 4.5 to 12 Gray (5Y 7/2) silt 6B 55 0 to 4.5 Brown (2.5Y 6/2) fine sand 4.5 to 10.5 | Gray (5Y 7/2) silt 7A 58 0 to 0.5 Gray (5Y 6/2) medium sand 0.5 to 10.2 (5Y 8/2), medium to coarse sand with <1.5-in-diam pebbles 8 50 0 to 13.8 Gray (5Y 6/2) micaceous well-sorted fine sand 50 0 to 4 (5Y 6/2) medium to coarse sand 4 to 13 Clean, coarse sand with ~ ° wy Cy WM fC WM & © ©& ~“ > e e Ce OO woo Hw © Oo © to to to to to to to to to to to to to to to to to to to to Description Gray (5Y 6/1) silty very fine sand Gray (2.5Y 7/2) fine sand Gray (5Y 7/1) silt-clay Brown (2.5Y 8/4), micaceous fine sand Gray (5Y 6/1) silt Brown (2.5Y 8/4) very fine to fine sand Gray (5Y 6/1) medium to coarse clean sand Gray (5Y 7/1) very fine sand Brown (2.-5Y 7/4) fine sand Gray (5Y 6/2) silt Brown (2.5Y 8/2) clean medium sand Gray (5Y 6/1) silt Brown (2.5Y 8/4) clean fine to medium sand Gray (5Y 7/1) silt Gray (2.5Y 7/2), fine to medium sand Brown (10YR 5/6), medium to coarse sand with very small pebbles Gray (5Y 6/1), clean medium to coarse sand fining with depth Grayish brown (5Y 6/2), medium to ccarse sand Gray (5Y 7/1), fine to medium sand Gray (5Y 6/1), clean medium to coarse sand Gray (5Y 6/1) silt Gray (5Y 7/2) silt Gray (5Y 7/2) silt, very fine sand Gray (5Y 6/1), silty medium sand with granules Tan (5Y 8/3), clean fine to medium sand Gray (5Y 5/1), silty medium sand Gray (2.5Y 6/2), clean medium to coarse sand Gray (5Y 6/1) silt Reddish brown (7-5YR 5.4), clean medium to coarse sand Gray (5Y 6/2) silt Gray (5Y 6.2) silt Gray (5Y 6/2) silt to very fine sand Gray (5Y 6/2), slightly silty fine to medium sand Gray (5Y 6/2) shelly silt Gray (5Y 5/2) silty fine sand Gray (5Y 7/2) silt . Gray (5Y 5/2) silty very fine sand Gray (2.5Y 5/2), clean medium sand Gray (2.5Y 6/2) silty fine to medium sand with organic fragments 60 Table A-2. Sediment description from cores in Long Island Sound.--Continued Core Noe | Water depth Internal (ft) (ft) Description Brown (2.5Y 5/2), clean medium to coarse sand Gray (5Y 6/2) silty fine sand Gray (5Y 7/2) silt Gray (5Y 6/2) silt, organic material at top Gray (5Y 6/2), slightly silty medium to very coarse sand with small pebbles Brown (2-5Y 5/4) medium to coarse sand Gray (5Y 6/2) fine sand, fining downward to gray silt Gray (2.5Y 6/2) fine to medium sand with broken shells and small pebbles Grayish white (2.5Y 8/2), clean fine to medium quartz sand Gray (5Y 7/2) silt Grayish white (5Y 8/2), clean fine to medium sand Light gray (5Y 7/2) medium to coarse sand with small quartz pebbles Brown (l10YR 8/3) fine to coarse sand with small pebbles 8 to 1l ft, becoming fine with depth Grayish white (5Y 8/2), very clean quartz, fine to medium sand Gray (SY 5/3) silty medium sand Gray (5Y 6/1) medium to very coarse sand with small pebbles Gray (5Y 7/1) silt Light gray (5Y 7/2), clean medium sand Gray (5Y 6/1) silty medium sand Gray (5Y 6/2) medium to very coarse sand Gray (5Y 6/2) coarse sand Brown (10YR 8/3), poorly sorted fine to very coarse sand with <1.25-in-diam pebbles 61 APPENDIX B RESULTS OF GRAIN-SIZE ANALYSIS This appendix provides a list of mean grain size and sorting for samples analyzed by sieving and settling-tube techniques. Sieve data were obtained by sieving samples at 0.5-phi intervals for periods of 20 to 30 minutes. Raw weights were used to calculate mean grain size and sorting by use of the method of moments. Settling-tube data were obtained by analyzing samples on the CERC Rapid Sediment Analyzer (RSA). The RSA method records at the top and bottom of a 1- meter-long plastic tube as grains settle through the water column through use of two pressure transducers. Pressure data are digitized and converted to equivalent size data of spherical quartz grains, and mean grain size and sorting are computed by the method of moments. Through comparison of the results of samples analyzed by both the RSA and sieving techniques, empirical relationships were developed for converting data obtained on the RSA to its sieve equivalent. These expressions, given below, were used to convert RSA means and sorting values to their sieve equivalents. Mean: = 0.1876 + 1.0735 dpoq $ Sieve Sorting: -0.146 + 1.453 S S sieve RSA Conversion between phi units and millimeters for grain diameters is pos- sible using the Wentworth grain-size scale (Table 4). The techniques are discussed in the Shore Protection Manual (U.S. Army, Corps of Engineers, Coastal Engineering Research Center, 1977) and Hobson (1979). 62 Table. wo wowo fo 6 6 OO HO WD & ee OO O25 © © 11 Sieve mean grain size and sorting values for selected core samples. Mean (phi) 2.19 0 1.23 =3 1.27 -4 0.41 -6 1.74 0 1.01 3) -0.30 -6 -0.19 -10 -0.20 0 2.45 =p 1.65 -8 2-56 B05) 2084 0 1.23 -2 1.34 —3 1.29 <7 0.97 102: 0.69 15) 1.82 0 1.26 —3 2.03 -4 1.97 -6 2.26 =I/ 1.39 -13.3 0.83 = 0.24 -6 -0.04 -8 0.57 -9 1.41 -13 2.54 0 1.81 il. 1.68 -4 0.95 -6 1.23 = 1.64 -10 1.14 Nit 1.31 mils} 1.08 Std. deve (phi) 0.88 0.96 1.19 0.85 1.05 0.89 0.79 0.75 0.92 0.69 0.95 0.37 0.67 0.80 0.91 1.07 1.31 0.99 0.98 0.81 0.64 0.50 0.57 0.56 0.68 1.35 0.67 0.96 1.36 0.86 0.80 0.85 0.57 0.63 0.60 0.48 0.42 0.72 63 15 20A 20A 20A 20A 20A 20A 21 21 21 21 Sediment depth (ft) Mean (phi) Std. dev. (phi) Wey dh}! 1.01 0.40 0.45 0.58 0.70 0.63 0.94 0.71 0.64 0.45 0.75 0.47 0.61 0.67 0.55 0.77 0.45 0.57 0.56 0.77 0.45 0.40 1.39 0.76 0.62 0.58 0.67 “0.85 0.56 0.99 0.72 0.60 0.62 0.89 0.61 0.78 0.74 Mean (mm) 0.86 0.55 0.26 0.39 0.49 0.49 0.22 0.55 0.36 0.76 0.51 0.34 0.25 0.62 0.76 0.46 0.66 0.42 0.51 0.54 0.77 0.42 0.46 0.60 0.56 0.64 0.53 0.47 0.29 0.26 0.40 0.39 0.38 0.33 0.26 0.30 0.54 Pace Table. Sieve mean grain size and sorting values for selected core samples.--Continued Core | Sediment} Mean Std. dev. | Mean Core | Sediment Std. dev. No. depth No. depth (ft) (phi) (phi) (mm) (ft) 21 -10.8 0.54 0.75 0.69 30 22 -7 0.77 0.94 0.59 36 22 -10 0.16 0.51 0.90 36 23 0 1.46 0.60 0.36 36 23 =) 1.56 0.41 0.35 36 23 -16 1.81 0.44 0.29 38 24 =3} 1.48 0.73 0.36 38 24 -6 1.16 0.56 0.45 38 24 -8 1.32 0.54 0.40 38 24 -12 2.09 0.70 0.24 38 25A 0 1.18 0.48 0.44 39 25A 0 1.34 0.33 0.40 41 25A =e 1.48 0.37 0.36 41 25A =] 1.50 0.34 0.35 41 25A -9.5 1.53 0.39 0.35 41 25A -14.5 1.53 0.34 0.35 41 26B 0 0.7/7 0.73 0.59 42 26B 0 1.36 0.89 0.39 42 26B 0 1.62 1.11 0.33 42 26B oil 1./0 0.61 0.31 42 26B 2) 1.42 1.09 0.37 42 26B 2) 2.16 0.89 0.22 43 26B -4 1.81 0.48 0.29 43 26B =5 1.64 0.34 0.32 43 26B -5 1.80 0.62 0.29 43 265 -7.4 2-10 0.54 0.23 44 26B -7.5 1.76 0.38 9.30 44 26B -10 1.97 0.51 C.26 44 27 0 1.13 0.81 0.46 44 27 -l 1.87 0.45 0.27 44 27 -4 1.94 0.42 0.26 44 27 —)q5) 1.27 0.70 0.42 45 27 -8 2.09 0.38 0.24 46 27 -11.5 1.08 1.04 0.47 46 28 (0) 0.75 0.63 0.60 47 28 =I 0.68 0.47 0.62 47 28 <2 0.77 0.42 0.59 47 30 -4 0.87 0.58 0.55 48 64 Table. Sieve mean grain size and sorting values for selected core samples.-—Continued Stde dev. | Mean Core Mean Std. dev.e| Mean Noe Sediment depth Sediment depth (ft) (phi) (mm) (ft) (phi) (phi) (am) 0.24 57 Alb: 1.44 0.47 0.37 0.15 62 0 -0.20 0.89 1.15 0.23 62 -5 0.78 0.67 0.58 49 0 0.60 62 -10.5 2.03 0.79 0.25 59 —3 0.37 66 0 1.62 0.55 0.33 50 -4 0.27 66 -10.5 1.31 0.57 0.40 50 -10 0.40 67A | -13 1.29 0.76 0.41 50 -15.5 0.26 67A | -15 1.71 0.84 0.31 51 -4 1.32 67A -15.5 1.85 0.45 0.28 51 5} 0.42 68 0) 1.01 0.20 0.00 51 -6 0.49 68 255) 2.72 0.67 0.15 51 -8 0.46 70 -4 0.34 0.67 0.79 52A 0 1.00 70 -6 224 0.78 0.85 52A 5) 1.16 70 —// 0.31° 0.69 0.81 52A -6 0.38 70 -8.5 0.39 0.73 0.76 52A -9.8 0.45 70 -9.5 0.28 0.58 0.82 53A 0 0.85 72 0 0.10 0.94 0.93 53A (0) 0.76 72 -4 1.42 0.34 0.37 53A Sil 0.63 72 7/55) 1.22 0.51 0.43 53A 205) 0.61 73 =5) 0.15 0.88 0.90 53A -3.5 0.54 73 -6 1.40 0.67 0.38 53A 5) 0.56 73 -6.8 1.29 0.44 0.41 53A -8 0.53 74 10} 1.22 0.65 0.43 53A -10 0.42 74 =] 1.02 0.79 0.49 53A -10.5 0.51 74 3365} 2.38 0.68 0.19 53A Siti 0.31 75 0 1.24 0.58 0.42 53A 12) 0.28 75 —]/ 0.94 0.65 0.52 53A 163 0.22 75 -13.4 1.09 0.40 0.47 53A -14 0.22 76 0 1.23 0.43 0.43 53A -15.3 0.46 76 5) 0.65 0.48 0.64 54 0 0.59 Ud —5 1.11 0.60 0.46 54 5) 0.53 77 -8 0.98 0.52 0.51 54 -4 0.58 77 -8.5 1.05 0.57 0.48 54 -5 0.40 78 0 -0.30 0.56 1.23 54 -6 0.37 78 ih -0.48 0,31 1.40 54 -7 0.29 78 <= ©.70 0.65 0.62 54 -12 0.56 78 —5) 0.79 1.07 0.58 57 0 0.71 78 -8.5 0.75 0.73 9.60 57 -6 0.28 65 Lé9 (Site “OARS EaATscne £02OL *saTiag “TIT “*sseayyer °S “SWETTTIM “II “98TITL “1 «*stsATeue --SjUdUTpes ouTIeW *z *settTddns pue quowdtnba--Sut{ [Tap 2109 °*T : *seare TeISeOD *S*y FO ABOeAeYD DTZ30TOSS ay Apnys 0] pue sad1nosei TaAeAS pue pues ai10YSJjJO ssasse 07 Saeak gt ysed ay. BuTANp (9YqD) TA}UeD YOIReSey BuTiseuTsuq Te seo) ay Aq pasn sai109 Jo saskTeue sy uo pue snjeiedde Suti0d Arz0j,eIQTA DTJeunsud ayq jo asn pue quowdoTeAap oy} uo uoTjeMAOZUT saptaoid jaoday *saduatTeJaI [TedTYdeAZOTTqGTq sepntTouT «*T86T ATDr,, *8TITI AsAOD (6-18 *ouU § pre TeoTuydeq BuTirseutTsue Teqyseoj)---wo /Z § *TTT : *d [gT] *T861 ‘SIIN Wory eTqeTTeAe : "eA SppTetysutadg { Jequeay yoresssy BuTAveUT3Uyg TeqIseo) Away *s°n : "eA SATOATOG JIOJ--*SWETTTIM SSeIFjJor *S pue a1edanqstow *q paeMpy &q / punog pueTs] Zuo] Jo rzaqoeVIeYD TeoTSoToes pue sadinosea pues *q paempy ‘a93anqstoy L£é9 (Fey POU eBqTscn* €O07ZOL *setias “III *sseirjjer *S “SWETTTIM ‘II ‘TITL “1 “*stsfyTeue --SjUdUTpas ouTIeW °Z *satT{Tddns pue juowdtnba--S8ur{{Tap 219 °*T spare [eqSeOD *S*y JO AaqJOeIeYD DTZo0ToOSs ayq Apnqs 03 pue sa0iInosei TaAeI3s pue pues siOYSFyJO ssasse 0} sieak gy 4sed ayq Butainp (94q)) JeqUeD YOIeeSey BuTAIseuTsuq Te}seoD |yR Aq pasn sai00 jo saskyTeue ayq uo pue snjeredde 3uti0d A10jeIGTA DTJeUNsud ay. jo osn pue quaudotTeasp ay} uo uoTJeMIOFUT SeptTAoAd jaoday *saouetejel Teotydeasot{qrq sapnzouy “186T Ate, *aTITI AeA0D (6-18 ‘ou £ pte TeoTuyde] BuTasseuTsue Teqjseo))---wd /z £ *TTT : *d [gT] “T1861 “SIIN Worzz eTqeTTeAe : "ea, ‘ppety38utads § aaquay yoAreassy ButTjoeuTsuq Teqyseo) Away *S°n : ea SAITOATOG JAO™¥--*SWETTTIM SSeaAsyer °S pue Jesingstew *q paeMpy &q / punog pueTs] 3uo] jo tazDeIBYD TedTSoToOes pue seoinoser pues *q paempy ‘iodangstoy Lc9 (=U) SOY BIT8cn* €072OL *seTies “III ‘“Ssseryjer *S “SWETTTIM “II ‘8TITL ‘I *stsATeue --SjudWTpes ouTIm *Z *settTddns pue jueudtnbe--Sut{[tap 39109 *] *spore [Te}SeOD *S*y FO TaqOeAeYD DTZOTOSS sy Apnas 0] pue sadinosei yTeaAeis pue pues si0ysyjo ssasse 0} sieak gt y4sed -284} BuTANp (9NgqD) e}UeD YOIeeSey BuTiseuTsuq TeIseoy) ay Aq pasn se100 jo saskTeue 9yj uo pue snjeiedde Sutz0d A10ReIGTA DTZeunsud 3yq Jo asn pue jusudoTaAep ayj uo uoTeWAOFUT saptAoad ja0doy *sauetleyel Teotydeaso0tTTqtq sapntTouy w*T86T Ato, *8TIT2 PAOD (6-18 *ou $ pre TeoTuyoe7 ZuTAseuTZue Teqseo))---wo 77 £ “TTT : *d [gT] “1861 “SIIN worzz eTqQeTTeAe ea, Spptetysutads § zaqua yoreosay BuTAseuTSuYy TeqIseoj Away *s*n : eA SATOATOG JAOJ--*SWETTTIM SSeIsJer *S pue ASesanqstow *q preMpy &q / punog pue,Ts] suo] Fo za}0e1eYD TeodTZoToes pue saoiInosea1 pues *d paempy ‘redainqstoy Le9 GQ. COu eaTssn* €02OL *seTies ‘III “sseasjyer °*S “SWETTTIM “II ‘“®TITL “I = *stskTeue --SjuauTpes sutTiew °z *settddns pue juewdtnbe--3uT{TTAp e109 *T *seore [eqISeOD *S*y JO JaqIDeIeYD DTZo0TOIas ayq Apnqs 0] pue seadinosei TaAeis pue pues ai0ysyjo ssasse 0} sieak gt ysed ay BuTanp (94ND) JeqUeD YyOIeesey BSuTiseuTsuq TeyseoD 9y, Aq pasn sarod jo saskTeue oyq uo pue snqeiedde 3uti0> A10}zeIQTA OT eWNeUud 242 JO asn pue usudoTeAep ay. uo uOoTJeEWIOJUT SaptAoAd jIodey *saduadejyea TedtydeasoTTqrq sapnyzouy w186T ATML,, *oTIT] JeA0) (6-18 *ou § pte TeoTuYyoe] ButaseuT3ue Teqseoj)---wo /z £ *TTT : °d [gT] “T1861 ‘SIIN Worz eTqeTTeae : *ea Sprtetx8utadg § taquay) yoressay BSuTiseutTsuq Teqyseo) Away *S°y : "ea SAITOATOG JIOq--*SWETTTIM SSeasjer *g pue Jesanqsteay *q paeMpy &q / punog pue[s] Zuo] Jo JeqOeIeYD TeOTSoTOes pue saoinose1 pues *q paempy ‘aradanqstoy DEC 16 gap