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@4 114-ko 46; 1 7- Coastal Zone information Ju Center Oil 77 IWK xg; 34%,; 4"t Tv ;A`* 4@ X; sr_ W-4 '14 31i @T, O#f 1'. .-to@@ 7,46, V - W Wt, A fib- Shore-fine and Bathymetric C h a n -!a -An the Coastal Area of Alaba at, A Remote-Sensing Approa,111 A, COVER: Alabama Coastal Area as seen from a 9@2 km (566 mi.) orbit by NASA's Landsat-I (image no. 1698-15490-7) on June'21, 1974, at approxi- mately 9:30 a. m. The image is filtered to emphasize the land-water con- trasts. Preparation of this Document by J. D. Hardin C. D. Sapp J. L. Emplaincourt, K. E. Richter Approved by: Philip E. LaMoreaux State Geologist and Off and Gas Supervisor Geological Survey of Alabama Remote Sensing/Topography Division SHORELINE AND BATHYMETRIC CHANGES IN THE COASTAL AREA OF ALABAMA A Remote-Sensing Approach COASTAL ZONE INFORMATION CENTER RELATED DOCUMENTS Alabama Development Office Alabama Coastal Area Program, 1974 Geological Survey of Alabama A Bibliography of Coastal Alabama, with Selected Annotations, 1974 Development of a Hydrologic Concept for the Greater Mobile Metropolitan - Urban Environment, 1973 The Environment of Offshore and Estuarine Alabama, 1974 History of Water Supply of the Mobile Area, Alabama, 1972 SHORELINE AND BATHYMETRIC CHANGES IN THE COASTAL AREA OF ALABAMA A Remote-Sensing Approach COASTAL ZONE INFORMATION CENTER Geological Survey of Alabama University, Alabama June 1975 Reproduction of this document in whole or in part by a user is permitted. The preparation of this document was partially financed through a Federal grant from the Department of Commerce, National Oceanic and Atmospheric Adminis- tration, as authorized by section 305 of the Coastal Zone Management Act of 1972. The program was administrated by the State Planning Division, Alabama Develop- ment Office, Office of the Governor. For Information Address: Alabama Coastal Area Board Alabama Development Office State Office Building Montgomery, Alabama 36104 First printing Printed in the United States of America Cover designed by Raymon d Rayfield and C. Daniel Sapp Unique Report Number: ALA-ADO-X996-CZMP-02 Abstract: The shorelines and near-shore bottoms of Alabama's coastal area are in a dynamic state, constantly adjusting to the combined effects of natural processes and man's intervention. Approximately 56 per- cent of the shoreline is eroding. Small amounts of erosion may be- come critical in developed areas. In general, erosion is of most concern along the western shore, at Dauphin Island, and along the north shore of Morgan Peninsula where waterfront residential areas are directly affected. Sediments derived from materials carried by the Mobile River system and by currents eroding the shorelines are gradually filling Mobile Bay. Computer analysis of bathymetry shows that the lower half of the bay is filling most rapidly, but the pattern of deposition is very complex. A NASA computer measurement of a part of the shoreline of Alabama used Landsat images and provided the basis for a preliminary esti- mate of the total shoreline length. This estimate is 1, 313 km (816 mi.), which is considerably higher than map measurements made by conven- tional means because the technique measures the intricate detail of upper estuaries and other shoreline indentations. CONTENTS Conclusions and re commendations ................................. Page Conclusions 1 Recommendations ......... 1 Introduction ........... 3 Objective 6 Methodology .................................................. 8 General 9 ............. 9 Shoreline changes ........................... 9 Bathymetric changes .................................. 11 Factors determining accuracy of results ........................ 11 General Accuracy of original data. ............. ................. 12 U. S. Coast and Geodetic Survey topographic surveys . @ ... 12 U. S. Geological Survey topographic maps .............. 13 Remotely sensed data ................................. 14 Cartographic procedure ................................... 15 Topographic charts ................................... 1 5 Aerial photographs ................................... 15 Accuracy of measurements and rate-of-change determinations. 16 Acknowledgements ........................................... 17 The milieu ....................................................... 19 Atmospheric ................................................. 19 Hydrospheric ................................................. 24 Bathymetry ...................................................... 36 Processes causing shoreline and bathymetric changes ................ 67 Winds, waves, tides, and currents ............................. 67 Severe weather disturbances ................................... 70 Sediment budget variations .................................... 72 Sea level changes. . ........................................... 73 Detailed assessment of shoreline and bathymetric changes ............ 75 Mobile delta ................................................. 76 Mobile harbor 8 1 Western shore ............................................... 82 Mississippi Sound, north shore ......... o ...................... go Dauphin Island area ........................................... 92 Eastern shore ................................................ 117 Morgan Peninsula, bay shore ................................... 121 Gulf shore ................................................... 123 Perdido Bay .................................................. 124 v CONTENTS Page Land/water interface analysis ..................................... 129 Measurement of Alabama shoreline length ...................... 129 Appendices ............................. 0... *... * ................ 136 A. Landsat imagery and hydrologic characteristics ....... * ..... 137 B. Source material and hydrologic data ...................... 0 0 149 C. Automatic processing of satellite data for shoreline meas- urement . . . o........ o ........... o. o o.. ... o...... o.oo.o.. 159 References.. o ........... o..... o ....... @_oo,ooo_..o_ ...... 160 vi ILLUSTRATIONS Page Figure 1. Location of study area .......................... 20 2'. Monthly precipitation characteristics for Mobile station 21 3. Mobile River drainage basin ........................... 25 4. Skylab-4 photograph .............................. .... . 27 5. Surface currents in Mobile Bay ..................... o... 28 6. Velocity directions for flood-tide flow predicted by a hydrodynamic model ............................ o ...... 29 7. Velocity directions for ebb-tide flow predicted by a hydrodynamic model ................................... 30 8. Landsat-1 band 5 scene taken on November 12, 1974, over Mobile Bay ...................................... 32 9. Landsat-1 band 5 scene taken on December 5, 1973 ....... 34 10. Major ship channels in coastal Alabama ................. 38 11. Rates of filling of Mobile Bay, 1852-1973 ................ 41 12. Mobile Bay bathymetry, 1852 ........................... 45 13. Mobile Bay bathymetry, 1920 ........................... 46 14. Changes in bathymetry in Mobile Bay, 1852-1920 ......... 48 15. Areas of deposition in Mobile Bay, 1852-1920 ............ 49 16. Areas of washout in Mobile Bay, 1852-1920 ...... ....... 50 17. Mobile Bay bathymetry, 1973 ........................... 51 18. Changes in bathymetry in Mobile Bay, 1920-1973 ......... 52 19. Areas of deposition in Mobile Bay, 1920-1973 ....o ....... 54 20. Areas of washout in Mobile Bay, 1920-1973 ........... - 55 21. Changes in bathymetry in Mobile Bay, 1852-1973 ......... 56 22. Areas of deposition in Mobile Bay, 1852-1973 ............ 57 23. Areas of washout in Mobile Bay, 1852-1973 .............. 58 24. Sampling transects for bathymetric profiles .............. 60 25. Mobile Bay bathymetric profiles 5 and 10 ........ - . _.. 61 26. Mobile Bay bathymetric profiles 20 and 30 ............... 63 Mobile Bay bathymetric profile 40 ...................... 1 64 28. Mobile Bay bathymetric profile 50 ...................... 65 29. Wind roses for coastal Alabama, January and July ........ 69 30. Shoreline changes in the Mobile delta region, 1917-1953 ... 78 31. Shoreline changes in the Mobile delta region, 1953-1967 ... 79 32. Changes in the rate of accretion for various time periods at the tip of the western natural levee of the Apalachee River, 1917-1967 .................................. 80 33. Areas of shoreline changes in Mobile harbor between 1918-1940 and 1940-1974 ............................... 84 vii, ILLUSTRATIONS Page Figure 34. Areas of shoreline changes in Mobile harbor between 1953-1967 and 1967-1974 ............................ 85 35. Changes in the rate of landfill for various time periods at McDuffie Island, 1917-1974 .......................... 86 36. Shoreline changes between Dog River Bridge and Fowl River Point between 1917 and 1967 ...................... 89 37. Rates of erosion at Cedar Point between 1917 and 1974 .... 91 38. Changes in the rate of erosion at selected points along the northern shore of Mississippi Sound ................. 94 39. Areas of shoreline changes at Dauphin Island between 1917 and 1942 ......................................... 98 40. Increase in occupance of a part of Dauphin Island between 1950 and 1975 ......................................... 99 41. Areas of shoreline changes at Dauphin Island between 1942 and 1974 ............................................. 101 42. Rates of erosion for various time intervals for Bienville beach and west-central Dauphin Island ................... 102 43. Rate of erosion for the western tip of Dauphin Island ...... 103 44. Bathymetric contours, Mobile Bay entrance and associated passes, 1929 ......................................... 105 45. Bathymetric contours, Mobile Bay entrance and associated passes, 1941 ......................................... 106 46. Bathymetric contours, Mobile Bay entrance and associated passes, 1961 ......................................... 107 47. Bathymetric contours, Mobile Bay entrance and associated passes, 1973 ......................................... 108 48. Sand/Pelican Island, 1975 .............................. 110 49. Changes in the configuration of Petit Bois Pass between 1848 and 1942 ............................................. 112 50. Changes in the configuration of Petit Bois Pass between 1942 and 1974 .............................................. 113 51. Bathymetric contours, Petit Bois Pass, 1917 and 1933 .... 114 52. Bathymetric contours, Petit Bois Pass, 1961 and 1973 - . - - 116 53. Rates of accretion at Village Point and erosion for an area south of Magnolia Beach ............................... 120 54. Shoreline changes in Perdido Pass, 1867 to 1890-92, and 1890-92 to 1918 ........................................ 126 55. Shoreline changes in Perdido Pass, 1918 to 1941, and 1941 to 1974 ............................................... 127 viii ILLUSTRATIONS Page Figure 56. Shoreline map showing limits of measured area from Landsat imagery dated December .28, 1972 .............. 132 57. Shoreline map showing limits of measured area from Landsat imagery dated December 5, 1973 ............... 133 ix TABLES Page Table 1. Hurricanes that have affected Alabama ....... ........ 22 2. Average tidal current velocities ............ 0.......... 27 3. Dredging in coastal Alabama ............... a.......... 39 4. Mean depths and rates of filling of Mobile Bay ........... 40 5. Area of landfill, Mobile harbor, 1917 to 1974 ........... 81 6. Filled areas in the Alabama estuaries .................. 83 7. Shoreline changes measured at selected identifiable points along the western shore of Mobile Bay ........... 88 8. Shoreline changes measured at selected identifiable points along the northern shore of the Mississippi Sound. . 93 9. Changes in area and average erosion rates for selected areas in Mississippi Sound ............................ 95 10. Amount of accretion at the western tip of Dauphin Island, 1917-1974 ........................................... 104 ii. Width and westward migration of Petit Bois Pass at various time periods between 1848 and 1974 .................... ill 12. Shoreline changes measured at selected points along the eastern shore of Mobile Bay ........................... 119 13. Shoreline changes measured at identifiable points along the gulf shore of Alabama .................. .......... 124 I i I " PLATES Plate 1. Historic trends of shoreline changes, Alabama coastal area, '1 1917-1974 . I I I - I I I I I I I . I I I I I 1, xi SHORELINE AND BATHYMETRIC CHANGES IN THE COASTAL AREA OF ALABAMA CONCLUSIONS AND RECOMMENDATIONS Conclusions The shorelines and near-shore bottoms of Alabama's coastal area are in a dynamic state, constantly adjusting to the combined effects of natural processes and man's intervention. Some segments of the shoreline have been armored or stabilized by seawalls and are no longer free to adjust naturally to maintain a state of dynamic equilibrium. Approximately 56 percent of the shoreline of coastal Alabama is eroding. This erosion varies from 0 - 1. 5 m (0 - 5 ft) per year to more than 3. 0 m (10 ft) per year. Small amounts of erosion may become critical in devel@ oped areas. In general, erosion is of most concern along the western shore, at Dau- phin Island, and along the north shore of Morgan Peninsula where waterfront residen- tial areas are directly affected. Erosion along the western shore averages 0. 97 m (3. 17 ft) per year. The maximum amount of erosion along the western shore occurs at Cedar Point which experiences an average of 2. 60 m (8. 56 ft) recession per year. At Dauphin Island there have been rapid and disatrous shoreline alterations caused by hurricanes, especially along the western spit. The northern shore of Morgan Peninsula between Seymour Bluff and Catlins Bayou has eroded an average of 52 m (170 ft) between 1917 and 1974. Although other shores show rates of erosion equal 2 to or greater than the rates affecting these areas, in most cases, those shores are uninhabited. Sediments derived from materials carried by the Mobile River system and by currents eroding the shorelines are gradually filling Mobile Bay. The lower half of the bay is filling more rapidly than the upper half, according to computa- tions based on soundings from nautical charts dated 1852, 1920, and 1973. Areas of most pronounced deposition are located in the upper bay where spoils disposal is occurring, and in the lower bay north of the tidal pass. However, the sedimen- tation pattern is very complex, with many areal variations that deserve further analysis Of the many passes and inlets within the changing configurations of the coastal area, the changing configurations of Petit Bois Pass, the Mobile Bay tidal pass, Perdido Pass, and Pass Drury were analyzed historically. Two of the larger passes, the,Mobile Bay tidal pass and Petit Bois Pass, appear to occupy the drowned channels of pre-Pleistocene rivers, and to be "pinned" in their positions; other smaller passes such as Perdido Pass and Pass aux Herons must be dredged constantly to keep them navigable, and former natural passes such as Pass Drury have been completely filled and have been relocated artificially. The length of Alabama's shoreline has been measured in various ways with a wide variety of tools. As a result, the true shoreline length is unknown; it has been 3 officially reported as anywhere from 491 km (305 mi.) to 1, 313 km (816 mi.). Manual measurements using maps and charts have omitted many intricate pat- terns of upper estuaries which should be included as part of Alabama's shoreline. The NASA measurements included in the present study were done by computer analysis of two satellite images of different dates, and yielded an average length of 1, 000. 4 km (621. 5 mi.) measured from the Mississippi line to 870421 W. (south of Foley. Measurement of the entire shoreline of Alabarna was not within the scope of this project. A ratio technique'provides an estimate for the total shoreline if done by this computer technique of 1, 313 kin (816 mi.). A final measurement of Alabama's shoreline will be done by NASA's Earth Resources Laboratory in the near future and the authors recommend that the results, when reported, be adopted by the Coastal Area Board as the total length of the state's shoreline. Recommendations This-assessment of shoreline and bathymetric changes in the coastal area of Alabama is concludedwith the follo wing recommendations: 1) A further study should be initiated which utilizes the oldest useable NOS (form- merly C&GS) topographic and bathymetric data available (approximately 1847) to determine shoreline and bathymetric changes over a broader s pan of time to follow up this report. As complete an inventory as possible of the past and present activities 4 of man in the coastal area should be included. This study would include establish- ing a baseline framework of geologic data for the coastal region. Suchmork was beyond the scope of the present project, since it would involve the geologic study of the sediments accumulated in the coastal area since sea level reached its present stand. 2) A 1975 coastal zone land-use assessment should be conducted and compared with the results of this study to determine what impact shoreline erosion has on com- mercial, transportation and residential shore land uses in the present and in the future. 3) A series of shoreline profiles should be established at selected points showing erosion, accretion, or dynamic equilibrium. The profiles should be redone semi- annually to establish short-term and seasonal variation so this monitoring activity should become a permanent part of the Coastal Area Board program. Summary technical reports on the short-term changes detected on the profiles and updated shoreline analysis using the latest remote sensing including automatic processing 6 of Landsat imagery for shoreline changes and land-use changes should be prepared annually. 4) The wetlands of the coastal zone. should be mapped in detail, using remotely sensed data augmented by field verification. The maps would be a valuable and 5 necessary complement to other physical and cultural (land-use) data to be gen- erated. This wetland study would include mapping of the inland/upland boundary and high-tide marks as indicated by plant communities. 6 INTRODUCTION The shorelines and near-shore bottom areas of coastal Alabama are con- stantly changing. This change is a result of both natural processes and anthro- pogenetic actions. Changes caused by natural processes may occur almost in- stantly, sometimes disastrously. High winds, waves, and extremely high tides generated by tropical storms and hurricanes may cause immediate and highly visible changes in the shoreline and near-shore bathymetry. In contrast, the rise and fall of the tides, wind and wave action, and the flow of tidal currents, active over tens, hundreds, or thousands of years, make their mark on the con- figuration of the shoreline and near-shore bathymetry slowly and sometimes im- perceptibly. Because these processes do operate so slowly, a single observer can only record a small part of the long-term changes they cause, and must rely on the existing written records of previous observers in the form of manuscripts, maps, charts, and photographs. In Mobile Bay and coastal Alabama, there are more extensive changes than those caused by nature - these are the changes caused by man's activities. Since the first colonization of the Alabama coast by the French in the early 1700's, man has been improving the bay by deepening natural channels; constructing wharves, jetties, groins, and seawalls; and filling in the bay to produce valuable real estate from the salt marshes. The effects of these constructions and repairs on the 7 shoreline and near-shore bathymetry are infinitely variable with location, type, and extent of construction. In some instances, construction may cause extensive changes in the shoreline and near-shore bottom configuration that are easily meas- urable over a short time span; in other instances, there is little or no discernible alteration. Changes in the shoreline and near-shore bottom can have great impact upon the navigation, fisheries, recreation, and residential uses of the coastal waters. Shoaling of important passes, inlets, and ship channels increase hazards to safe navigation and incur high costs of sediment removal and disposition. The depo- sition of sediment over viable oyster reefs can cause the loss of a valuable fish- ery resource and mean loss of livelihood to many coastal fishermen. Shoreline erosion may mean increased expense for seawalls, groins, or)--evetments to the recreation cottage owner or permanent resident, not to mention the impairment of scenic vistas caused by such constructions. Valuable waterfront property may be lo st and buildings damaged or destroyed by shoreline erosion. Many residents and the sports fisheries suffer when a tidal inlet such as Perdido Pass is partially obstructed and rendered unsafe during rough weather. Great expense is incurred on the part of local, state and federal governments to construct jetties and seawalls to control sediment deposition. 8 Shoreline erosion and near-shore bottom changes are not simply subjects of academic interest, but are subjects of great concern and interest to the many people of Alabama's coastal area who are directly or indirectly affected; but, the question remains, how much, how long, and for what reason do these changes occur? Objective The objective of this report is the documentation of the direction and magni- tude of the movement of the coastal shoreline and changes of near-shore bottoms of Alabama through the use of vintage nautical charts, National Oceanic and Atmos- pheric Administration (N. 0. A. A.) topographic sheets, U. S. Geological Survey topo- graphic maps, air photos, and satellite imagery. Primary interest has been placed on those trends measurable since the early 1900's, but in some instances trends have been analyzed from the mid-1880's to the present. This project is unique in that it brings new techniques to the solving of prob- lems in a relatively small but dynamic area. Paramount among these new tech- niques is applied remote sensing, encompassing a group of surveillance techniques including aerial and space photography; and computer cartography using the SYMAP program. 9 Much of the more recent data utilized in the study represents the state of the art in remote-sensing technology. Sources such as multispectral Landsat-1 imagery, space photography, high-altitude and low-altitude color infrared photog- raphy, conventional black-and-white aerial photography, and thermal infrared imagery have all been carefully analyzed. A complete listing of the types and dates of all data used in the research is provided in appendices A and B. A gen- eral discussion of atmospheric factors precedes the shoreline and bathymetric presentation. Methodology General Historic shoreline and bathymetric change assessment requires the col- lection of all available data concerning past shorelines and bathymetry. These data include vintage and recent nautical charts by the National Ocean Survey; vintage maps by the French colonists; topographic surveys by the.U. S. Geologi- cal Survey; and all available air photos and remote-sensing imagery, including Skylab and Landsat-I imagery. Shoreline Changes Understandably, the available data are of various accuracies and scales. For analysis of shoreline changes, the usable data were reduced to a common 10 base. - The base selected was the latest'CJ. S. Geological Survey 7-@'@-minute topo- graphic sheets (1:24, 000) or earlier U. S. Geological Survey 15-minute topographic sheets (1:62,500) for areas where the former were unavailable. Whenever possible, opaque prints were converted to positive transparencies at a scale suitable for use in the K & E Kargl photo- rectifier. This machine was used to reduce or enlarge data to the scales of the base maps while simultaneously allowing for the correction of small distortions inherent in the original data. Where prints could not be converted to transparencies, a Focalmatic desk projector (opaque projector)was used to transfer the shorelines to the base map. Once the selected data were compiled at the base scales, segments of the resulting shoreline configu- rations were quantitatively analyzed to provide information concerning the linear extent of shoreline erosion or accretion and, where appropriate, the area of land lost or gained. All areas were measured with a polar planimeter. At selected locations identifiable on the base maps (U. S. Geological Survey topographic sheets), the total change of the shoreline was determined and the rates of change for various intervals of time were calculated. In some areas the average erosional rates were determined by planimetering the area of erosional or accretional change for a par- ticular shoreline segment and dividing this figure by the length of the shoreline seg- ment. Bathymetric Changes National Ocean Survey charts of Mobile Bay containing hydrographic surveys for the years 1852 (Coast Chart no. 188, published in 1856), 1920 (U. S. Coast and Geodetic Survey no. 1266, published in 1921), and 1973 (U.S. Army Corps of Engi- neers Navigation Maps of Gulf Intercoastal Waterway, New Orleans, LA, to Apa- lachee Bay, FL, map 6, 7, and 8) were used to conduct an analysis of bathymetric changes in Mobile Bay and vicinity. A 0. 5' latitude by 0. 5' longitude grid was super- imposed on each of the three charts. The depth of water at each grid intersection on each chart was interpolated and stored on punch cards. A computer program called SYMAP, developed by the Laboratory for Computer Graphics and Spatial Analysis, Harvard Center for Environmental Design Studies, Graduate School of Design, Har- vard University, Cambridge, MA, was used to produce 12 maps showing the bathy- metry, the areas of deposition, and the areas of washout between 1852 and 1920, 1920 and 1973, and 1852 and 1973. Factors Determining Accuracy of Results General Assessing long-term shoreline changes by comparison of vintage National Ocean Survey (formerly U - S. Coast and Geodetic Survey) topographic sheets, U. S. Geological Survey topographic sheets, and remotely sensed data, all at differing scales, mapping detail, and accuracies, must obviously introduce some question as to the accuracy of results derived from these data. Aside from the accuracy 12 of the original data, there may be problems in interpreting shorelines from aerial photography or other remotely-sensed imagery, and there certainly are carto- graphic difficulties in compiling data using different datums or lacking horizontal control, and in transferring shorelines to a common base, Once all data are com- piled on a common base, there are limits to the accuracy of measurements of shoreline changes and determinations of average changes and rates of change. Accuracy of Original Data U. S. Coast and Geodetic Survey Topographic Surveys The degree of accuracy of the early surveys depended upon the purpose of the survey, its scale and date, the standards for survey work then in use, the relative importance of the area surveyed, and the ability and care that the indi- vidual surveyor exercised in his work (Shalowitz, 1964). However, a high degree of accuracy does not necessarily mean a high degree of detail; this depended upon the importance of a shoreline area to the purposes of the survey, as seen by the surveyor. Thus, in many shoreline areas, shoreline segments were sketched in between surveyed control. This is especially true of marshy areas where, of necessity, the outer edge of the marsh and not the actual high water line was mapped, as in cases where details of minor tidal creeks were omitted-. In gen- eral, the horizontal accuracy of the mean high water line on the early surveys is within a maximum error of 10 m (33 ft) and may possibly be much more 13 accurate (Shalowitz, 1964). After World War II, photogrammetric mapping tech- niques further increased the accuracy of the survey. In summation, Shalowitz (1964), states: There is probably little doubt but that the earliest records of changes in our coastline that are on a large enough scale and in sufficient detail to justify their use for quantitative study are those made by the Coast Survey. These surveys were executed by com- petent and careful engineers and were practically all based on a geodetic network which minimized the possibility of large errors being introduced. They therefore represent the best evidence available of the condition of our coastline a hundred or more years ago, and the courts have repeatedly recognized their competency in this respect .... U. S. Geological Survey Topographic Maps The U. S. Geological Survey publishes 7. 5-minute (1:24, 000 scale) and 15- minute (1:62,500 scale) topographic maps, which were used in this study. Under the U.S. National Map Accuracy Standards for maps at scales smaller than 1:20, 000 (which includes both the 7. 5-minute and 15-minute maps), 90 percent of all well-defined features, with the exception of those unavoidably displaced by exaggerated symbolism, will be depicted within 0. 50 mm (1/50 in ) of their 14 geographic positions as referred to the map projection (Defense Intelligence Agency, 1967). On a 7. 5-minute topographic sheet, 0. 50 mm (1/50 in) is equivalent to 12 In (40 ft) on the ground. For a 15-minute map, this accuracy is equivalent to 31.7 m (104 ft) on the ground. The preceding accuracies are minimum standards and are greatly exceeded in most cases. Remotely Sensed Data Actual photographs, such as the prints and transparencies used in this study (app. B), are subject to various sources of distortion or image displacement. Ob- jects on aerial photographs may not be registered in their current horizontal posi- tion because of optical or photographic distortions, tilting of the camera lens axis at the instant of exposure, or variations in local relief (Avery, 1970). Errors due to optical aberrations or photographic deficiencies were small and needed no special corrective measures for the purpose of this study other than normal care to use only the central area of the photographs. Tilting of the camera lens axis was corrected by making the appropriate scale adjustme nts along the axis perpendicular to the tilt axis of the photograph with a K&E Kargl photo-recti- fier while transferring shoreline data to the base maps. Because the study area is of low relief, the effects of relief displacement were negligible. Aerial photographs at scales ranging from 1:20, 000 to 1:130, 000 were used in the study (app. B). The smaller scale photographs (1:130, 000) presented some 15 problems in the interpretation of the land/water interface, and at this scale deter- mination of the salt marsh/water interface was somewhat arbitrary. There was no problem in differentiating sandy beach from water, because the contrast be- tween the two was always great. Cartographic Procedure Topographic Charts Original plane-table surveys used by the Coast and Geodetic Survey to com- pile navigation charts included shoreline data overlayed on a 1-minute grid. Posi- tive prints of these data were converted to positive transparencies or autopositives at scales near those of the 7-1- or 15-minute topographic maps, on which a 1-minute 2 grid had been drawn to facilitate transfer of shoreline data. The photorectifier was then used to project the data onto the bases, while simultaneously allowing for corrections and "fitting" of data necessary because of minor distortions gen- erated in the various photographic and duplication processes. Aerial Photographs The geometric inaccuracies of aerial photographs required some corrective photogrammetric triangulation to determine shoreline locations where ground con- trol was available. The lack of ground control or identifiable cultural control in many areas (notably Mississippi Sound and the Mobile delta) precluded the use of aerial photography in determining shorelines in these areas. 16 Although the cartographic procedures used in this study may have introduced some errors in the transfer of shoreline data from the topographic charts and aerial photographs to the topographic map base and then to the final illustration, the major emphasis of the procedures used was the correction or diminution of errors inherent to the original maps and photos. Accuracy of Measurements and Rate-of-Change Determinations Measurements of linear distances on maps were made to an accuracy of 0. 25 mm (0. 01 in), which is equivalent to 6. 0 m (20 ft) on the ground for a map at 1:24, 000 scale or 15. 8 m (52 ft) for a 1:62,500-scale map. An optical comparator with a 0. 5- mm reticle was used for all shoreline changes and most rate-of-change determinations. This type of measurement often produces a higher order of accuracy than the original data warrants. The determinat ion of rate-of-change is subject to certain limitations. The intervals between surveys and remote-sensing coverage are erratic, rates of erosion or accretion must be assumed to be linear between the dates of shoreline measurement, and multiple rates can be obtained at any one shoreline segment using various combi- nations of lines (Brown and others, 1974), or by fractionally shifting the location of the line of measurement. 17 De spite these limitations, the method of assessment of long-term change and rates-of -change in the shoreline using charts, maps, and remotely sensed data rep- resent the most practical method now available. The user of this stuVs results should realize that the limitations of the methods of measurement used require that emphasis be placed on the general trend of shoreline change, with the measured change and rate of change being of secondary concern; in other words, is shore- line erosion occurring at a low rate or a relatively high rate in a given area, or is there apparent equilibrium in a given area? An appreciation, by the user, of the limitations of the methods used in this assessment will ensure that the results of this study will be both significant and useful to the proper management and development of the resources of the coastal area. Acknowledgements The authors appreciate the assistance and cooperation of several individuals in various organizations. The shoreline computer measurement work was done by Kenneth Faller at the Earth Resources Laboratory, NASA Johnson Space Center. The authors would also like to thank John Cammack of the Geological Survey of Alabama and Edmund German of the U. S. Geological Survey for their help in the coordination of the SYMAP computer program. Some of the information dealing with suspended sediment in Mobile Bay was kindly provided by Allen Kerr and 18 Dewayne Imsand in the Hydrology and Hydraulics Branch of the U. S. Army Corps of Engineers in Mobile. Read Stowe, professor of anthropology at the University of South Alabama, provided ancient maps of Dauphin Island. 19 THE MILIEU Atmospheric Located between 30' and 31' N. latitude at the northern end of the Gulf of Mexico (fig. 1), Mobile Bay is characterized by a warm humid subtropical cli- mate, with somewhat high temperatures from April through October and mild winter months. This type of climate mainly results from 1) the latitudinal posi- tion of Mobile Bay and its eastern location in relation to the North American land- mass; and 2) the effects of two dominant air masses, the warm moist tropical air mass originat ing from the gulf and the cool dry continental polar air from central Canada. Of importance to the coast are the amounts of precipitation, seasonal trends, and hurricanes. Precipitation totals at the Mobile station average 173 centimeters (cm) or 68.1 inches (in) per year. Monthly characteristics are illustrated in figure 2. There is no well-defined seasonal trend such as a dry winter or summer period;. however, there is a noticeable difference in that the precipitation decreases during the fall. Monthly or seasonal differences in precipitation affect the discharge of the Ala- bama River into the bay and consequently affect the depositional /erosional rate at the same time. Hurricanes have played a pronounced but infrequent role in altering or sha .p- ing the shoreline. Table 1 lists the dates of hurricanes that have affected Alabama Ge rgetown'. ro N nter ak G e b u Minetl Hurricane Wil or Q 4f 30abu Cl) S 0 rol ts ry I 0 I Semmes Chic A VL 0 Big Creek . e @ 201 ake @2I Stapleton @ 0 -3A- Ga esi voo V. Steelwo@ 0 Spanish Fort an I fillso MOBILE 0 Mal is 181. P25) McDuf ie 1 0 Iyall. Village Pt LoxI y .8 40 Dog River Pt Daphneo Ragged Pt Belf est 5 Montrose jack n The M 0 B I L E S@ Iv. @hillo obert ale JairhOpe rvin n S Imo efontaine Battles Wharf M rdal .11 --- - Great Point Clear Point Clear lay City Grand Bay 0 Fowl River Pt ro Mar ow LA ixon Mon Louis orn er B A Y M agn lberta !-;ij3iftr Delchamps @T Mullet Pt Weeks Spri g Fole Bay c- Bay Gr&pd Alabama Port 81 Isle Aux Herbes 0 eron Bay 21 er ido Beac Zt- phine Bon Secour 0 Barron Pt Cedar Pt 0 0 a S 0 D Bay Bon e our ranj WATERWAY r Bay MISSISSIPPI - - - - - - - - - - - - T LNLR ;OAST@@L -4t- Dauphin Is, "-@Little Point Clear - - -:@ - Pelican Gasqu F r P in @;efic'a n @ @@,l s @Ia, up nd Pelican lsland@@ Bay Little LagOu" k Pt Sand Island4 M G L 0 F in '@o @''a Figure 1. --Location of Study area. Gomm 21 25 ANNUAL TOTAL 10 17 3.04 CM o r 68.13 1 N 9 2o- 8 j:j:j:. 6 15- ............. ........... ..... .......... ............... .5 ............... ......... ::X .......................... ....................... 23K, ... ... ....... ......... 10 j:. -Ki: .. . ... . . .... _3 .... ...... .. @%xxx ............... ....................... ... ...... 3 ................. . . ........................ ......................... .......... .................. .....% ......... .. "XiX ................ 2 5. ..... ......... ............X K-3. -K'. . . ....... ... ........................ .... . ...... ... . ........... ... . .......... Cm. IN. Figure 2. --Monthly precipitation characteristics for Mobile station, 1941-1971 (Brower, Meserve, and Quayle, 1972). 22 in the past 75 years. Note that these storms all occurred in August, September, or October, except for the July hurricane of 1916. Sixty-five percent of the hurri- canes occurred during September. A hLirricane affects Alabama's coast every 52 months, on the average. The specific effects of these storms upon the shoreline and bathymetry will be discussed later, as appropriate. Table 1. --Hurricanes that have affected Alabama* Date Remarks 15 August 1901 Landfall, Grand Isle, La. 27 Sept. 1906 Very destructive - wind intensity of 150 kph (94 mph) at Fort Morgan. Landfall, Pascagoula, Miss. 20 Sept. 1909 Landfall, Grand Isle, La. 14 Sept. 1912 Landfall, Mobile, Ala. 29 Sept. 1915 One of the most intense. Landfall, Grand Isle, La. 5 July. 1916 3. 25 m (10. 8 ft) tide above mean sea level at Mobile (2. 3 m (7. 5 ft) at Dauphin Island and 3. 4 m (11. 2 ft) at Gulf Shores). Landfall, Gulfport, Miss. 18 Oct. 1916 Landfall, Pensacola, Fla. 28 Sept. 1917 Waves overtopped the seawall at Fort Morgan. Land- fall, Pensacola, Fla. 20 Sept. 1926 One of the most destructive - 48. 2 cm (19 in) of pre- cipitation recorded at Bay Minette. Landfall, Perdido Beach, Ala. 23 1 Sept. 1932 Landfall, Mobile, Ala. 19 Sept. 1947 Very destructive - considerable damage near the mouth of the Dog River. Landfall, New Orleans, La. 4 Sept. 1948 Landfall, Grand Isle, La. 30 August 1950 Mainly affected the Fort Morgan-Gulf Shores area (Hurricane Baker). Landfall, Mobile, Ala. 24 Sept. 1956 Hurricane "Flossy" mainly affected Dauphin Island. Landfall, Ft. Walton Beach, Fla. 15 Sept. 1960 Hurricane "Ethel" - no serious damage. Landfall, Pascagoula, Miss. 3 Oct. 1964 Hurricane "Hilda" caused beach erosion from Point Clear to Mullet Point and along the Fort Morgan peninsula. Considerable damage reported at Dau- phin Island. Landfall, Franklin, La. 17-18 August 1969 Hurricane "Camille" - very destructive storm. Tide at Pass Christian rose to 6. 8 m (22. 6 ft) above mean sea level. Landfall, Waveland, Miss. Source: Report on Hurricane Survey of Alabama of Alabama Coast, U. S. Army Corps of Engineers (USACE) 1965 and 1970; and Chermock, Boone, and Lipp, 1974. 24 Hydrospheric Mobile Bay receives the waters from the fourth largest river system in the United States. The Mobile River system (fig. 3) drains approximately 112,966 square kilometers (km2) or 43, 650 square miles (mi. 2) and discharges a mean annual 1, 764. 8 cubic meters per second (m3/s) or 62,316. 8 cubic feet per second (ft3/s). Another mean annual discharge of 3.55 m3/s (125. 6 ft3/s) enters Mobile 1 Bay below the Battleship Parkway from Montlimer Creek and Fish River (Crance, 1971). The movement of the outgoing water through the bay has been examined (Austin, 1954) and shows that during a 6-day period in October 1952 (period of low river discharge) the river discharge moved primarily on the western side of the ship channel. Moreover, Austin states that 85 percent of that discharge passed through the Mobile Point inlet directly into the Gulf of Mexico, while the remaining 15 percent flowed through the Mississippi Sound outlets. A more recent study (Lamb, 1972) indicates an increase in salinity in the Mississippi Sound area which would probably change the percentages for movement of the discharge. It is probable that the building of the bridge system from Cedar Point to Dauphin Island (plus the subse- quent sedimentation) has diverted some fresh water from the Mississippi Sound, thereby increasing the salinity (Lamb, 1972). However, some of the Landsat-1 imagery (for example, November 17, 1973, pass in appendix A) seems to confirm 25 09 MOBILE BAY 5@0 1 0 0 0 190 270 KM Figure 3. --Mobile River dra inage basin. 26 Austin's results. Thus, it is apparent that the circulation pattern within the bay warrants further field investigations. Figure 4 .illustrates the flow pattern of discharge through the bay. This Skylab photograph was taken on January 21, 1974, at about 3:00 p.m. local time. The light tones (as opposed to the darker tones) show the suspended sediment being carried out of the bay and illustrate the direction of flow very well. January 1974 experienced an unusually high monthly discharge with a mean of 5,869. 6 m3/s (207,259 ft3/s). Only three oth,er months of January have exceeded this mean dis- charge since 1929. The January 1974 discharge represents about a 222 percent increase over the mean for that month (app. B). Mobile Bay has diurnal tides that vary from 36 cm (1. 2 ft) at Mobile Point to 45 cm (1. 5 ft) at the mouth of the Mobile River. An extreme high tide of 3. 24 m (10. 8 ft) above mean sea level was recorded during the July 1916 hurricane and an extreme low tide of 3. 15 m (10. 5 ft) below mean sea level was measured during the 1926 hurricane (Crance, 1971). Tides, river discharges, the bottom configuration of the bay, and water move- ment deflected due to the coriolis effect all contribute to the circulation patternswithin the bay. Average current velocities associated with the flood and ebb tides vary between 15 cm per second during flood tide at the Mobile River entrance to 77 cm per second at Mobile Point during ebb tide (see table 2 for the velocities in different parts of the bay). 27 Figure 4. --Skylab 4 photograph -(SL4-63-392) taken with the S190A camera over Mobile Bay on January 2i, 1974, at 3:00 p.m. local time or 2 hours before high tide. The light tones within and south of the bay indicate suspended sediment discharging into the Gulf of Mexico. Table 2. --Average tidal current velocities (diurnal in centimeters per second@ Location Flood tide Ebb tide Main ship channel entrance 36 52 Mobile Bay (off Mobile Point) 72 77 Channel, 10 km (6 mi.) N. of Mobile Point 31 26 Mobile River entrance 15 36 Tensaw River entrance 21 36 Pass aux Herons 67 67 From- U.S. Coast and Geodetic Survey, Tidal current tables, 1969, in Ryan and Goodell, 1972. 28 According to Ryan (1969), during flood tide the incoming water that passes through the Mobile Bay tidal pass first deflected to the east, and then northward in a counterclockwise direction (fig. 5). However, a recent study of a hydrodynamic and salinity model for Mobile Bay (Hill and April, 1974) indicates different results. Taking in consideration that the wind vBlocity is zero, the inflow and outflow pro- Jiles are.shown in figures 6 and 7. OCT. 1952 OCT. 1952 EBB TIDE FLOOD TIDE 6 After Austin 1954 in Ryan 1969 Figure 5. --Surface currents in Mobile Bay. The ship channel has altered the natural circulation pattern by introducing a salt-water wedge up the entire length of the bay. Both the Tombigbee and Ala- s bama River discharge about the same quantity of sediment into the bay. Certain variations exist between the two rivers during certain periods of low and high dis- charges. Appendix B, table 4, indicates the amount of suspended sediment for a period of 12 years. 29 f I I I f Ar -4- Figure 6. --Velocity directions for flood-tide flow predicted by a hydrodynamic model (after Hill and April,1974). (:VL 61 III-TdV pur IIIH J@IJ13) IaPOLU ouu-euSpoapS@q u Sq pajoT I poad A',OTJ app-qqa JOJ suOT 30-11P AIIDOIOA-- L ojn@3ij AFF /4 I f t f t 0 c 31 Satellite imagery has proven to be a very useful tool for the study of sed- iment patterns. In July 1972, NASA launched its first Landsat-1 satellite (for- merly ERTS-1) into a near-polar orbit. This was the first satellite dedicated entirely to the study of the earth, and its track passes over Alabama every 18 days. The multispectral scanner (MSS) subsystem on the platform images the earth's surface in four different bands of the electromagnetic spectrum. These four bands are as follows: Band 4 0. 5 to 0. 6 micrometers wavelength (green) Band 5 0. 6 to 0. 7 it fl (red) Band 6 0. 7 to 0. 8 It (near infrared) Band 7 0. 8 to 1. 1 (near infrared) Suspended sediment transported by streams and rivers is quite visible on Landsat imagery and can be easily traced in the sea. For example, the Landsat-1 band 5 image of November 12, 1974 (fig. 8), illustrates very nicely the sediment plume extending approximately 20 kni (12 mi.) into the Gulf of Mexico. This image is of particular interest because the ship channel forms a boundary between-the heavily sedimented eastern part of the bay and the less sedimented western part of the bay. Such a pattern is contrary to the findings of previous studies on circu- lation patterns within the bay; however, it probably resulted from unusual conditions because patterns on most other Landsat-1 images seem to follow the earlier findings. Noted also on this November 12 image is a large amount of sediment off the Mississippi 32 ro A j "Nor Oj -A @4 4r -it @x 4 7;, Mr (Ar Figure 8. --Landsat-1 band 5 scene taken on November 12, 1974, over Mobile Bay. Unusual sediment patterns appear higher on the eastern side of the bay instead of the western part. High amounts of sediment transported by the Mississippi River appear off the west side of Chandeleur Island. Also well outlined is the concentra- tion of suspended sediment on the northern side of the Mississippi Sound Islands, ,., km which supports Austin's results on the circulation pattern. 33 River delta. Low tide in this case occurred approximately an hour and a half after the image was recorded. A December 5, 1973 (fig. 9), image shows unusual patterns not only within and off Mobile Bay, but as far as 60 km (40 mi.) southeast of the Mississippi delta. Again, in this case, low tide was about two and a half hours before the multispectral scanner recorded the image. A series of Landsat-1 band 5 images, along with tidal graphs, current veloci- ties, and river discharge, is provided in appendix A. The seasonal trend of the amount of suspended sediment (which is actually a function of river discharge) going out of the bay can be observed on the imagery dated 1972 to 19174. Throughout this 2-year. time sequence tidal stages varied widely, and it is very apparent that tidal circulation dictates the transportation pattern of the sedi- ment. In case of unusually high discharge, the tidal mechanism seems to be over- ridden, as illustrated in the case of the--January 20, 1974, Skylab photograph. From the Skylab and Landsat-1 scenes, several observations concerning suspended sediment can be made: 1) suspended sediment is clearly visible on the imagery; 2) the amount of sediment is usually associated with the discharge char- acteristics of the Alabama - Tombigbee Rivers; 3) the boundaries between sedi- mented and less-sedimented waters can be drawn as far as 100 kin (64 mi.) out into the Gulf of Mexico; 4) there is a definite sedimentation concentration onthe 34 _K Figure 9. --Landsat-1 band 5 scene taken on December 5, 1973. The image dis- plays large amount of suspended sediment detectable as far as 100 km (60 mi.) southeast of the Mississippi River delta. 35 northern side of the Mississippi Sound Islands. This represents not only discharge of sedimentb.y other streams, but also confirms Austin's study stating that about 15 percent of the sediment from Mobile Bay flows through the Mississippi Sound outlets; 5) general patterns in the current directions can be inferred; 6) the long- shore westward current is detectable on most of the imagery. For sediment studies, band 5 (red) Landsat-1 imagery is found to be the best for the detection of sediment distribution patterns. 36 BATHYMETRY Mobile Bay is about 50 km (31 mi.) long, 13 km (8 mi.) wide in the north, and as much as 38 km wide (24 mi.) wide in the south. It is nearly blocked from the Gulf of Mexico at the south by the Mobile'Point barrier and Dauphin Island. A second outlet (and inlet) is Pass aux Herons, between Dauphin Island and Cedar Point. The bay measures approximately 1, 0 15 km2 (392 mi@ ) in area. Mobile Bay is a geologically young estuary. In fact, most estuaries are young, ephemeral features, having been formed by the last eustatic rise in sea level. Mobile Bay has probably held its present outline and shape from the time of its formation several thousand years ago; however, thebay is filling with sedi- ment. The characteristic pattern of estuaries is to fill most rapidly near the head (delta) and progressively fill up in the move distant reaches. This pattern can be altered by changing rates of sediment influx from rivers and streams, relative changes in sea level, tidal circulation, and climatic changes. Man's influence, also, is an important factor. Within the next thousand years, Mobile Bay will probably become an alluvial -deltaic plain similar to the present delta. The contemporary configuration of the bottom of the bay is essentially flat and sloping southward. The dredging of the 12x122 m(40x4OO ft) ship channel has increased the relief down the center of the bay, and the dredging of the east-west 37 intracoastal waterway has had a similar effect in an east-west direction across the widest part of the bay (fig. 10 and table 3). These changes are confined to narrow corridors, but there are also other changes in configuration due to more or less natural causes. These "natural" causes may ultimately be man-induced rather than otherwise, and they involve differential sedimentation and erosion rates. The bay was deeper in 1852 than in 1920 or 1973, as table 4 indicates. The rate of filling between 1852 and 1920 was 0. 49 m (L 63 ft) per 100 years. This rate decreased to 0. 52 m (1. 68 ft) per 100 years between 1920 and 1973. These figures are for the entire bay and were obtained by taking the mean of a systematic sample consisting of 1, 720 soundings taken from National Ocean Survey charts. It is illuminating to divide the bay into two equal parts, the northern half and southern half, and compute the mean depths for the same three dates. Table 4 shows the results. The filling of the upper bay is decreasing, whereas the filling of the lower bay is increasing (fig. 11) - The rate of filling of the upper bay was 0. 58 m (1. 91 ft) per 100 years between 1852 and 1920, but this rate decreased to 0. 30 m (1. 00 ft) per 100 years between 1920 and 1973. This decrease is significant but its cause is unknown. The construction of dams on the Alabama River and other tribu- taries in the Mobile River drainage basin may have trapped sediments that would c GARRO.5 SEND CHANNEL 2P X 150' HOLLINGERS ISLAND CHANNEL IV X 175 THEOD RE CH0 40' X 4000' (PRO"" J MOBILE BAY BAYOU LA SATRE CHANNEL 11' X 100' MISSISSIPPI SOUND %5V INTER COASTAL WATERWAY INTER COASTAL WATERWAY 12' X 125' DAUPHIN ISLAND BAY CHANNEL 7' X 40' PERDIDO PASS CHANN x BAR CHANNEL SCALE 1:250,1300 Figure 10. --Major ship chann @.o 39 Table 3. --Dredging in coastal Alabama AREA DATE VOLUME Gross cubic meters Gross cubic yards Mobile Outer Bar March 1975 215,813 (283,965) June 1974 185,683 (244,320) July 19 72 199,482 (262,476) Perdido Pass July 19 74 303,616 (399,495) Sept. 1972 289,122 (380,424) July 1971 183,888 (241,958) Fort Gaine s Aug. 1974 12,261 16,133) (Mobile Bay Nov. 1972 54,098 71,182) tidal pass) Nov. 19 74 34,023 44,767) Pass Heron March 1969 1,141,319 (1,501,735) (Pass aux Herons) Bon Secour July 1974 303,616 (399,495) (Bay) Oct. 1966 45,203 ( 59,478) Oct. 1964 590,713 (777,254) NOTE: All dredging jobs do not start and finish at the same point year after year; therefore, the volumes dredged vary greatly. Source: U.S. Army Corps of Engineers, 1975 (written communication). Table 4. --Mean depths (MLW) and rates of filling of Mobile Bay TOTAL BAY MEAN DEPTHS RATES OF FILLING 1852 1920 1973 Change 1852-1920 Change 1920-1973 Change 1852-1973 10. 71 ft 9.60 ft 8. 71 ft Filled 1. 11 ft Filled 0. 89 ft Filled 2. 00 ft (3.26 m) (2.92 m) (2.65 m) (0. 33 m) (0.27 m) (0. 60 m) Rate 1. 63 ft/100 years Rate 1. 68 ft/100 years Rate 1.65 ft/100 years (0. 49 m/100 years) (0. 51 m/100 years) (0. 50 m/100 years) UPPER BAY 8.90 ft 7. 60 ft 7. 07 ft Filled 1. 30 ft Filled 0. 53 ft Filled 1. 83 ft CD (2. 71 m) (2.31 m) (2. 15 m) (0. 39 m) (0. 16 m) (0. 5.5 m) Rate 1. 91 ft/100 years Rate 1. 00 ft/100 years Rate 1. 51 ft/100 years (0. 58 m/100 years) (0. 30 m/100 years) (0. 46 m/100 years) LOWER BAY 12. 52 ft 11. 59 ft 10. 35 ft Filled 0. 93 ft Filled 1. 24 ft Filled 2. 17 ft (3.81 m) '(3. 53 m) (3. 15 m) (0. 28 m) (0. 37 m) (0 - 6 6'm) Rate 1. 36 ft/100 years Rate 2.34 ft/100 years Rate 1. 79 ft/100 years (0. 41 m/100 years) (0. 71 m/100 years) (0. 54'/100 years) 41 2 LL ----,,LOWER aAY 10- Z @@WHOLE UI UPPER a z Uj 5- 1852 1920 1973 Figure 11. --Rates of filling of Mobile Bay, 1852-1973. 42 have otherwise reached Mobile Bay. One can also speculate that there has been a decrease in land under cultivation, a resulting decrease in erosion, and there- fore a decrease in suspended sediment load carried by the rivers The lower bay shows an increase in the rate of filling from 1852 to 1973. Between 1852 and 1920, it filled at the rate of 0. 41 m (1. 36 ft) per 100 years. Between 1920 and 1973, this rate increased substantially to 0. 71 m (2. 34 ft) per 100 years. As with the upper bay, the initial causes of the rat e change during these periods is not known but is subject to speculation. The increase in sedimen- tation in the lower bay might be attributed to dredging of the east-west intracoastal waterway, the widening and deepening of the ship channel*, or the relatively recent construction of the Dauphin Island causeway" across one of the bay's two outlets. In any event, as table 4 shows, the lower bay was only 3. 15 m (10. 35 ft) (mean) deep in 1852. Ryan (1969) compiled isopachs of the bay and cites sedimentation rates in excess of 1. 2 m (4 ft) per 110 years in the delta area. In Bon Secour Bay he shows rates of 0. 6 to 0. 9 m (2 to 3 ft) per 110 years. His results are consistent with the Th e ship channel was constructed between 1826 and 1857 to a depth of 3 m (10 ft). Between 1870 and 1934, the channel was deepened and widened periodically and reached its present dimensions between 1955 and 1957 (Ryan, 1969, p. 38-39). Construction of the causeway was completed in the mid-19501s. 43 findings of this study. Ryan (1969, p. 68) states that Bon Secour Bay appears to have the highest natural sediment accumulation rate. The findings o f this study differ: the bottom north of the bay entrance, east of Dauphin Island, has the high- est sediment accretion rate; whether this deposition is natural or is man-induced spoil is debatable. In any event, the highest rate of deposition is not in Bon Secour Bay. The distribution characteristics are discussed later, along with the SYMAP computer maps of bathymetry. Ryan does write that the entire bay has an average accumulation rate of 0. 5 m (1. 7 ft) per century, a finding confirmed by this study. Ryan (1969) does not report a decreasing erosion rate for the upper bay, how- ever. He emphasizes man's role in increasing the sedimentation rate in the upper bay, and cites rates of greater than 0. 9 m (3 ft) per 100 years in the area immedi- ately south of the delta. This may be the case in isolated areas, but this study finds a lower, decreasing rate 0. 46 (1. 51 ft) per 100 years for the upper bay during the 1852-1973 period. To summarize the bathymetric findings of this phase of the study, the rate of filling of the upper bay is decreasing, while the rate of filling of the lower bay is increasing. Overall, the bay is filling at the rate of 0. 5 m (L 65 ft) per century. There is no reason to expect any change in this trend in the near future. As a result of the filling, Mobile Bay will shrink in size and the delta will prograde southward. 44 A discussion of the statistical means of bay depths provides only a general picture. For details, computer plots of bathymetry were generated using the Harvard Uni-iversity SYMAP program. These maps originated from soundings .tabulated from National Ocean Survey charts . A grid having a 0. 8 km (0. 5 mi.) spacing was used for systematic sampling of bathymetry for the three dates 1852, 1920, and 1973. These maps, eachhaving 1, 720 sample points, were interim steps for synthesis of a derivitive set of maps showing change between the dates 18 52-1920 and 1920-1973, as well as 1852-1973. For each date and period, the bathymetry of the bay will be discussed, the salient changes will be described, and the changes will be divided into depositional and erosional components. Figure 12, entitled "Mobile Bay Bathymetry, 1852, depicts a flat, rather featureless estuary before the effects of man had become evident. The greatest bay depths were at the tidal pass between Dauphin Island and Mobile Point. The central area of the bay measured 3-6 m (10-20 ft) in depth, and the mean depth for the entire bay measures 3. 3 m (10. 7 ft). Figure 13 shows the bay in 1920. Its. character is considerably differ ent, and the effects of dredging (spoil) are evident. Much of the west-central part of the bay is now only 1. 5-3. 0 m (5-10 ft) deep, which is only half as deep as in 1852. 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IXIAIIIIIIIIIIIIXII x................... 11 III-XII, IXIXXIIIIII .1 X@ X. . ..".11I.XXI T.XX ..........XX.,X...Xx.:.X.Xl@'..:,.X.X.X...,.:@I 1. 1 : 1. 1. 1X, T , , @ XF lX l , @ l . . ,FF @ l X X @ X - X FF X XX a ,X X l l X , ll l x xx x x x x XT x x x x x x x x x x Ax xx x x xxF lxF l l . . . . . .FIXIIXXX X.- .. . ... :*.. ........ XI._XAT.-T. . . I. . ox N. 1XI., XII.I. x . xx . 11 1, 1 I.Xl Ix . @11 X 1. "X.Xl IXI.I.X I., x IN, X .IX .1 I.IX:1 I: Ixo:I@,.F1xxx: IXI. IIx ::X.'I.Ixxx@IxIa:I@I. I.: FX: X.: To.X . . . . . . .X..KIXe -XIF . . . . . . .. . . . . . ...... I-IXXIII [email protected] ...... I I I . I I111 XIIX 1:-:..:X, xx:.::.X" 11 X. . KX. l-.-I.X..xx .. X:1.1. .1. X-l.., . . . . lx, x:"xxx :Ixlxxl". I. . . . . . . . . . . . . . . . . . . . . . . . . .x-.,X-:Ix.II .1.11:1. 1-1. I.X-XX-XII-..X:.XIx N .,xxlxxo-x.-. ...... ::::::%X XIXXAXXXXXXIIKIXI@,.@XIIXI@.,[email protected].@. . . . .xx . . . XXXXX 1XIIIIIX IIIIIIIXIIKIIIIIIIXI X 111111 . . . . . . . . . . . .F.Ixxxx XXIIXIII I.X.:.. 11.1 IIXIIIIII.X@ X_ . . . . . . . . . .X_X. XI.X IX IXXXXI XIIIIXIIIIXXXIXIIIX"Ill"""XXKXXK --1XII Xle. . . . x .. X.Xxxxxx ........ x @'lXF'.:@X . . . . .X:..XAXI.':.:XX: IXIIXII-xa xx . . . . . . . . . . . . . . . .. . . . . . . . xx:I.I.XIII:IX:llX.I..XXXI.I: xx X, _X .... ......... X..-.-.X.X.,Xx I. . . X. . . .X. .._o . . . . . . :**::::::::*,*****'+**************** ............ ............ -:::::.,XA@x:,Ax.xxxlx:xxxxxKxxxxxxxxxxxx@xxxxxxxxx":Xx,:,X:,A"XA:xxx@xx@xxxxxx:x@,xx:xxxx:4xxx:xxx:xxxXXX4:xxxxxxxxxxxxxxAxxXAXXXX:xx:xxxxxxxxxxxxxxxxxx"xx)xx:xxxxxxxxxXXXXAXXXXXXXXXXXX,x . xx . . . . . . . ......:. . . IXXIXX:Xlx:"Ixx"",XXXXI.X,..AX.'@'..1.:XXXX:.X"XX'IX.".Xx:.X@x:.,.X.X.@@"*::::::::::::::::::::::::::::::::::*::::::::::::::::::::::::::::::::: x:"..X....,AX . . . :.--.XX-X-.%.A":--X-X T: xx -::-:,X.:@-x-x,--.,x . . . . X...X,.X; X.X.,...:X:.X.X.:.:@,[email protected]'.X- X eX. X.X . :x xx XI X. lX IX Tx- -X . . .X.X . . .-...,X. -.X-;x:..-:xx.-;x- -F . . .X..X... xx.. [email protected]@[email protected]@[email protected]@.X.:@...@ ...... X....X:@x.:X.:..Xx....Xx:..:,X:...:.X.-X.... X..X X.,X:x... xx,.XXxxxxxxxxxx. ........ ... ...-....X ....... .. ........... XXXXXI-1--Txx . . . . . . . . .o.. :.X.X,.Xx.: . . . . . . . . . .X., . . . . .X,X"X"xx,xx,x"x . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . K. . . . . .xxx.xxxxgAx toe xxxxxx lllxx., . . . xlx:x,:TIo'IX.Il.XXXXXXX . . . . .x I I I IXXXIIIIINXXXXX . . . xxex . . . I X I X X .11 X. ,I X. INXI. IXXXI. F. F XX . I-x o :11.1.1:lxxl @XIXI-XI-XXI@XIIIXX@IIXIIXIIIIXAIIIIXIIXXX o ..F ... X-l ... ..... 1. Ix @, ,I: XX@,XX.I.X.IXXXXIXI.I.IX 1. exxxx Ix IN . X..". Gooo-eaf "X'XX"X'XXXXXX'XXXXX'X"X"[email protected]@XX :.Xl @,:X IXNXXXXXIXXle,.X....XXl. x. . . ...Xx . . . . . . . . . . . . . . . . . . . . . xxxxxxxx@ ...... xx,.::, '*""** a .... -x ... x,,xxxxx..."@.",X.X,.Xxx".X"..xx .... T xx .- XX.Xxxx. x.... .... "xx,x..x . . . . . . . . ::::::,*,.Xlx"x:..:X.:,.Ixx..X"IXIXX"""Xxxxx . . . . . .. . .F- . . . . . . .X.- . . . . . . . . . . . . . . . . . . . . . . . . .:**** . . . . . . . . . . . . . . . . ."IF .. X..Xa . . .x. . . .X..Xx.:: . . . . . .:+:::::::*.:::::::: ..::::: . . . . . . . . . . . . . . . . . . . . @XI.Xlllxl.:"",:"Xx.:.X:xxx,:..:-:@xx..:: .ea X--X-xx:xx:--x-:--:::: . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . -ex:x- .. X.,X.xx.. . . . . . . . l.. . . . . xx . . . . . . . . . . . . . . . . . . . Xxx l.. X.l. #68#eo#o Ixx,xl"-- X. ... X.. x . . . . .Xl . . . . . .X..... . . . . . . . . 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N .... .......... ..................... .. llxlxxllxl.,.@IXIIIXI.;X:I.Xlxllxx.:X@lllxx:x. :::::::,FIX .1.1 ... .............. .......... ..... .................................................... ........................ . ..... ..... - .x-.... .. . .:.. .::::...:.Xxx,.:: ....X...x . . . .:.-GaGaGoota.se . . . . . . . . .xx. .. . . . . . . . . . . . . . . . . . . . . . . .... . . . . . . . . . . . . . . . . . . . . . . . . . . to . . .e. . . . . . . . . . . . . . . . . . . . . .. . . .X... xx.x. . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ..... . . ....... ........ . ..... ... ...... .... ...... ....... ... - .. ..... ...... .... . .. ...... .... ... 1. .4 ... ... ....... .. ..... ...... . ... ........ .... ....... X. .... ..... ... ......... ...... .... ... .......... .. ... ....... .... ........... ... ... ....... ..... .......... .... .......... ..... xx,- . ............... ...... ".1 ..................... .............8........................ ................ ....... ........ I.......................... .......................................... Figure 12. Mobile Bay bathymetry 1852 ........ .. .... . .. .... .... ........ . ...... ... ...... . ...... . . ...... ....... ... . ..... ... ... .......... ....... ....... .-....... ........ ............... ....... ................ . ......... ...... ........... *-- ... ....... . ....... ...... ..... . ................... .. ........................ .............. .... x** "'. 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X.Xxxl ......... ......... X. l 11 llI.lXXX@N.'l-'Xl lN.XA'%* l: X . . . . . . . . . . . .... ......... ......... x- lxl --x X-l.:l ......... ....... .lx, llx ... : xx.--l- "xx":",. --l ... X. l:l. ......... ...... lxxx..l .. lxx. xx .... ...... . . . . .xlI.-xx----l-. ...Xx.. X. x lX:xx.-X:X-l..:@-,l . . . . . . . . . . . . XXxl X- . . . . . . .. ..... . . . . . . . . . . . . . . .x... . ....... :..:,.X....X .......... xx ...... . . . . . . . . . . . . . . . Ix . . . . .xx X..Xxl.:Xx ..... . . . .X..X . . . . x.... l.. ............ x , , x ,x : x , , x x , x , x x , , x , , x x x x , x , x , , x , x. . . . . . . .xxxxx,,,x,x,,_ll., 'X ... -- ...... "XX""",X""""",,X""XXIIXIIXXXIII"XIXI""X"X""'I .-lIA .. l.,.X.X.-X..- .. x ... I........ X.-N.... .. X.I.X..X .. X..X.X..:,X:xl""""Xl".XxIllxl:,.:,X:,.,:.:Xl:I .... l.llxx. l.-I-XII.... ::X.,xlIx . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. ........ .... ... llIX.IX.X..X.AX .... ll ..... X. ... ... X..X.XXXl ...........X....................................... ... ...... -XII X.X XXX .:::*XlllllXlllXAXllll 11 ... l, XXXl .....XX.... .. X... . . . . . . . . . . . . . . ll . . . . . . .xx . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .l. . . . . . . . . . . . . . . . X XX I "IllX"",X"XlllXll,"X"I"""Xl",XXXXIXIXXIXXXIII x XX,,X, '.N' x K, x xxx xxxxxxx "xx'x x"Nl" x I.IN"XI.I., Ix ll lXI.IXIX x 1. .1 x l., x NX, I.,. lX.XX x I.. XI.X . X. . .XI..:,*: 1. . . . . . . . . . .l. CK ...................... . . . . . . . . . . . . . . . . . . . . . . . .......... ....................... ..... . . . . xx..Xx ........ .X:.x :,Xx::.-.-@-,,x . . . :.::.X..X..Xx . . . . . . .X.AX....Il . . . . . . IIIIIXIAXI IXIIX IllII I I I . . . . . . . .l.....l. . . I . .ll . . . . . . . . . . . . . . . .l .. 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I.N., .. ........... l .::::.x......................... .: . .. ::. - :. - .::..:x .. xx:x X.x ..........a............ ........................... ... . ....................... ........... :: ...... :: . .......a............ :: ......... . ... .....n. xl ..... .. .... ..... xllx . . ... ....... .X.xx ................... ens z........B.................................................. . ... . ............................... .... ::.. .... . ...... ............... .... . . .. . ....... ........ .... .... .. .......... ................................................................. ............................... ....... ............. ............. ........ . ..................................... ... ...... ... ........ . ...... . ..... ..... .. ...... .............. ........... .............. .... ............. .............. . ..... ............. x...IXXxx .. x .. X" x"XIIII, X.... ........................... x ........................ I.............7 ........... ............................ 4... .......4 .... 4....................................................... ..... ................................. ..................... . I ..... ................................ .. I. .................. .... ............................... ....... ............. ........ ........ 4 .......... .......I.. - ........ . ......... - - l................. ................. ..... ..... ..... ............... . . ... ............... ........ I.......... .. ............ ............. . . ... ............. .................. ............. ............. .... ...... ............... ............ ........ .............. ................ ........... . ....... .............. .... ....... ... . ............ ... ........... .... ..... Figure 13. Mobile Bay bathymetry 1920 mmm-mm m m 47 this 68-year period. The tidal pass to Mobile Bay remains, however, the deepest water. Figure 14 is a computer- derived comparison of the two bathymetric maps, and shows filling as well as washout (erosion) of the bottom. The "difference map" reveals filling in the main entrance (outer bar), as well as in small isolated location east of Dauphin Island, in the center of the bay, and generally east of Mobile city. The south-central part of Mobile Bay experienced 0. 3-1. 0 m (1-3 ft) of filling during this period. Figure 15 shows only the filling (positive values) and thus sim- plifies the patterns considerably. The areas of washout, 1852-1920, which are represented as negative values, are illustrated in figure 16. This map reveals that there existed few areas of washout, submarine erosion, or scouring in the bay. Figure 17 shows the present (1973) Mobile Bay bottom configuration. The bathymetry is now complex, quite unlike the patterns of 1852 and earlier. The effects of dredging show as a more or less continuous north-,south trending ridge 1. 5-3.0 m (5-10 ft) deep at mean low water (MLW). This ridge widens at the 'lati- tude of Cedar Point but tapers in again and deepens quickly to more than 12 m (40 ft) at the main entrance. The upper bay immediately south of the delta is now shallow, averaging only 1. 5 m (5 ft) deep or less. Much of the bay off the city of Mobile has been filled, and there is little bay area left deeper than 3 m (10 ft) now. Figure 18 shows the computer analysis of differences. The greatest deposition I , ;.. ... .-I ,;;:: 11 I : :,I'll .. .. .. it 1:::: t; I 1. . ":::: :::::: it:: .- @;i::::::;::;:::: . .,.-.\ ..:. .1 ... . . .. it . . Q:::: 11:II11 .11 :: ::: V, ;; . 1.-. :::; i: it it it it-I. 11 it it :: 11 it :: it :: ..1. . N I :: ". 1. 1. .it it 11.III.@ " "" ,. ,L ". ,'.'., iiii it it it it it-@..,-, , I *,@, i; . .-Z. it it " ,it it% it, :: !: .. 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Changes in bothymetry in Mobile Bay 1920-1973 - =@- -@ --' ** @-- -:=@- --, @:- - -- - ` P.-P.- == --:- ---2 -----@- ; ..XXI.. - :- -@ ---- @@ .......* I I I - --- 53 occurred in four areas: 1) off Mobile city, 2) east of Dauphin Island, north of the main entrance to the bay, 3) south of Dauphin Island, and 4) north of Little Point Clear. Each of these areas is of limited extent, but the filling is signif- icant, on the order of 3 m (10 ft) addition to the bottom during the 53-year period. Figure 19 shows only the areas of deposition (1920-1973), and figure 20 shows only the areas of washout during the period. The latter map reveals three areas of erosion of J. 5-3. 0 m (5-10 ft) magnitude: 1) off Mobile, 2) in the tidat pass, and 3) in the gulf bordering Mobile Point. Three additional computer maps illustrate the overall change in bathymetry from 1852 to 1973. Figure 21 shows both deposition and washout. This map is divided into positive and negative components (figs. 22, and 23). The positive pattern (fig. 22) is dominant, and the salient difference is the dredging along the ship channel. This ridge of spoil is evident from the main entrance all the way -to Mobile. Each end of this ridge is raised even more, so that about 3 m (10 ft) of filling has occurred in these two locations. Figure 23 shows the overall nega- tive pattern (washout) during the 121-year period. Most of the scouring has occurred in the main entrance of Mobile Point, but other significant areas of washout are in the upper bay off Daphne (Ragged Point) and the Blakeley River bar. Eastern Bon Secour Bay shows as much washout as it does deposition; in other words, little overall change is evident in this area. xxIIxI Nx.: ...... xxxI x ............... I"'INIx" ........ ::t Ix xx .,..xx .xx:IxI.:xI. .11 xx x x,.x.xxx x Ix xx t..x I INT. 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XIxx XXF . ..X - XIXXXI .,X..XXI.,.,X,.,.::Ixxxlxl@X."I IIIIXIIX X, x". . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . xx x mxm 1 04-464-86. IIXXII x"XII . xx. IIxxxxxI 11 XXXXX.:... x:@Illlxxlxx.@x:..,..".X,..*:::::::::::*:::::::*.,..X@l*:::: NXIN xxx. X.XXXIIX.X"X .. Ix ... IX xx.,..x'.'.'x .... NxxxIxIIx .... ... ..... F xxx 11-9 a*:::: -xxx.- :.X,.::* .xx -Xkv!4, x. ........... -IIxXI -i- IXI ...-XIXX "-, I X= ,,,x xWx,x ..... .. ...... x.... I IXXI.I.XX.. x... x e.x .. .... ..... X, + IXIIIXIX ............ I.. XxX..X .... XX.xXX.X.X X. Ixx xXI..,.IXXl :111 ...X.. ..... I.::. xI XIIIIII X.,:::, 11 X, . . .x - X ... .... ... ..... .. xx. ... . ........ xx 11 .. Nx.XXXI.I.I.I.4.: .. ...... xx,xx.* ...... XXI xx *0 xx X.-14 :::* ... Xx :*.",X,.*:. .1 .......x... X. ..x xx .... xx. XXI.N.I.I.N.I.I. N. ,X,.", X .,**.X.,.,.XXI.I.X..X.I.Xl ..... ... .. X.x X. x .. X..,...X. X.xI .... .. Ix ..... X.X.x X "W"I", X..X.. xxIxxxI XX .. xxXXIII,X ..... .................. 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"IXX X xXXIxXI.I.I:.I.I:,x . . . . . . . xx.... x X..X.X .............. ... xx..X,X...x . . . . . . . . . . . . . . NXXXXXXIXX . ..x 6 X.. . xx .......... .......... ............ .......... ... ... ... .. Xx .......... ...... x- x x .. Figure 19. Areas of deposition in Mobile Bay 1920-1973 ---------- . ..... ... . . ----------- ------ ---- - - - - - - - - - - ----------------- --- - - - - - - - - - - - - - - - - - - - - - - -- --------------------- ------- -- ----------------- ------------------- ---- -------------------- - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - PERCENTAGE OF TUTA, I-E RANGE APPLIIIG TO "IN LIIEI - ------ ------- ---------- --------- ---------- ----- ----- --------- --------- ......... .... .... .... 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Areas of depos-ition in Mobile Bay 1852-1973 PERCENTAGE OF TOTAL -E-7E 1-1 OAIGE AP-21G TO EICH LEVEL 33. 36 13.31 LIVE!, - - - - - - -=Z@===Z7=-@ ---------!--------- --- ------------------------------------ ---- ------ -- ---- 'ELI' 1 1.1 -11 1@1 @l Ol .1 1 . 11 co - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - 77- . ... ...... . --------- - ----- ---- -- --- -- -------- -- ------- ------ --- ------ ---- -- - --- ------- ------- ---------------------- --- ------- - ------ ------ ------------ - - ------------------ --------:------ - -- - --- - - --- ---- ---- ----- ------------------------- ---- ------- --------------- -- .. - - - :::: =---2 === ::: :::::: ------------- ------- - Figure 23. Areas of was-hout:in,Mobile Bay 1852-1973 59 A more detailed discussion of the bathymetric changes in passes of Mobile Bay and Mississippi Sound is provided separately in the section on shoreline changes. These details were obtained by contouring the soundings at larger scale. The com- puter-derived maps just described consisted of "smoothed" and interpolated surfaces that tended to obscure details but provided an excellent and objectively generalized picture of the whole bay. The SYMAP original graphics were produced on a 97 by 77 cm (38 in by 30. 5 in) format and subsequently reduced photographically to 33 percent of this size for illustration in this report. The originals are on file at the Geological Survey of Alabama, Remote-Sensing Division. A discussion of the bottom configuration of Mobile Bay is not complete with- out some information on profiles. A series of six east-west profile s was plotted from soundings from National Ocean Survey charts dated 1852, 1920, and 1973*. The graphs were made by averaging soundings for 0. 8 km (0. 5 mi.) grid squares and plotting profiles of the averages across the bay. Figure 24 shows the location of the profiles and figures 25, 26, 27, and 28 show the profiles, presented in order from north to south. The northernmost profile (line 5, figure 25) reveals the man-made accretion immediately south of Mobile during the entire period 1852 to 1973. This accretion * The hydrographic data for each chart are not renewed each time a chart is compiled, but instead the National Ocean Survey apparently adds new soundings continually. It is not possible, therefore, to fix the compilation date of the hydrographic data for these charts, and these three general dates must suffice. Go r9ot .0 M 6a ter sk G Minetl H rroicane r S r 04f.,0 edbary Cr all Sernmes hic A(' L f I N i C g Creek r "I ke P Stapleton Steelww G+si wood 0 Spanish Fort n I s 0 0. r MOBILE 5 maltos 5 0 5 0 NE 5 Village PtT 0 Lox1 ey H4 10 41 Cr I aphne. 41? ,,o Ragffod Pt Bel est 0 Montrose j&ok The 0 Fairhope Af O'B IL A rvingt n S t Imo are" Point clear Battles Wharf 0 merdal Grav d Be Fowl River Pt Point Clear lay City @y 0 a ow ixon ner -30 -:-- @ -- @ Mag 0@lberta ftaiAlft Delchamps 0 Mullet Pt Weeks Spri v Fole C@. Bay Bay 0 40 21 Isle Aux H er ido, Beac C) 0 Bon Secour Phine Barron Pt Cedar Pt Bay Son our W1 Ba MISSISSIPPI SoUIqD WArERWAY - - r Bay Or. COAST@_L--'-'@ 50 Dauphin Isl Z@ -- 4-@ ra Peliran/ Fo Gasqu M', ,zz@_ Daup in and Pt ulf Shores S, 'Pelican Paiiar, lvand,4, Little Lagoon Bay M.Ml. Pt Sam I$I&nd4 G U L F o F Fiw 24 R mrQi trawts Wat)wtri 1 61 0 WESTERN SHORE SHIP CHANNEL EASTERN SHORE 5 10 1973 1920 1852 LINE 5 15.- _j F- 20 4. LLJ LLJ LL_ 0 F- CL SHIP CHANNEL LLJ 5 A \V/ 10 LINE 10 20 5 10 15, 20 25 30 35 GRID INTERSECTION NUMBER Figure 25. --Mobile Bay bathymetric profiles 5 and 10. 62 seems to be increasing somewhat, as the change is greatest after 1920. Line 10 (same figure) shows a continuation of the accretion west of the ship channels. Further south, the distribution of the filling becomes more even across the bay, as line 30. (fig. 26) illustrates. Moreover, this part of the bay filled most during the post-1920 period. Yet, farther south, line 40 (fig. 27) shows a continuation of this trend. The filling is of greater magnitude than the previous line shows, but this increase is in proportion to the widening and general deepening of the bay to the south. Most of the change in the middle of the bay occurred before 1920, ex- cept in the vicinity of the ship channel. The shelf fringing the edges of the bay is spreading towards the center but the bay bottom remains predominantly flat in this area. The bottom configuration further south, across the widest part of the bay, is radically different than that to the north, as line 50 (fig. 28) reveals. This profile runs from Dauphin Island to Oyster Bay. The ship channel area, which is plotted in the vicinity of grid intersection numbers 12-17, has filled several feet, according to the graph, but the resolution of the grid does not permit plot- ting of the 40-foot dredged channel itself. The graph depicts only the general depths in the ship channel area for each date. Most of the fill is probably spoil from channel dredging. An overall filling trend is indicated immediately north 63 WESTERN SHORE EASTERN SHORE 5 SHIP CHANNEL 10- 1973 1920 LINE 20 1852 15- 20 LLJ LLJ U_ 0 uj SHIP CHANNEL 10 15- LINE 30 20.4 0 5 10 15 20 25 30 35 GRID INTERSECTION NUMBER IP CHANI Figure 26. --Mobile Bay bathymetric profiles 20 and 30. WESTERN SHORE EASTERN SHORE 0- 5- SHIP CHANNEL U-i LU NO DATA U_ 10. 1973 1920 LLJ m LINE 40 1852 15- 20 -------------- 3 @0 5'0 55 0 5 10 15 20 25 0 @5 45 GRID INTERSECTION NUMBER `@P Figure 27. -,-Mobile Bay bathymetric profile 40. WESTERN SHORE EASTERN SHORE 0- LITTLE DAUPHIN ISLAND 5. <c LLJ U.J U_ SHIP CHANNEL 1973 1920 LU in LINE 50 1852 20 1 @0 0 5 10 15 ;0 310 i5 510 5'5 GRID INTERSECTION NUMBER Figure 28. --Mobile Bay bathymetric profile 50. 66 of the Mobile Bay entrance as well as in Bon Secour. Bay south of the intracoastal, waterway. 67 PROCESSES CAUSING SHORELINE AND BATHYMETRIC CHANGES Shoreline and bathymetric changes are a result of complex interactions among natural -processes and, often, the activities of man. The apportionment of the effects@ of @ each natural process on a specific historical shoreline or near- shore.bottom,. or even on an existing one, is a most difficult problem requiring extremely detailed data. This information does not exist at this time for Mobile Bay. Observations can be made, however, on the general effects of natural and anthropogenetic processes as they operate within the coastal waters of Alabama.' Changes result from the normal interactions of winds, waves, tides, and currents severe. weather disturbances; sediment budget variations; and sea level changes. Winds, Waves, Tides, and Currents Winds may cause extreme variation in the normal tidal range in Mobih and Perdido Bays, and Mississippi Sound. Waves generated by winds having a long fetch can impinge upon a windward shore and cause much erosion in just a few hours. Wind- generated longshore currents and rip currents may quickly remove and transport shore materials from an exposed shoreline. In the coastal area of Alabama, average wind directions andvelocities vary with the seas ons During the fall and winter months, winds are predominantly from the north or northwest, while spring and summer winds are from the south or southwest (Cher- mock, Boone, and Lipp, 1974. In January, 19 percent of the winds are from the north 68 octant and 14 percent are from the northwest oct-ant (fig. 29). Velocities may range as high as 13.3-28. 0 km/hr (12-20 knots). In June, 15 percent of all winds are from the south octant and 14 percent are from the southwest octant. Velocities may range as high as 13. 3-28. 0 km/hr (12-2 0 knots) (Institute for Storm Research, 1974). The average annual wind direction and velocity is from the north at 13. 3 km/hr (9. 5 knots) (Cranee, 1971). Persistent high winds from the north and and northwest during the winter months tend to depress the water level in much of the bay and concurrently cause a buildup,of waves along the south and southeast shores where wind fetch length is great. Under these conditions, severe erosion may occur along the northern shore of Morgan Peninsula. During the summer months, and occasionally in the winter months, per- sistent and strong south and southwesterly winds cause a decrease in water level, especially in the lower bay. Waves and tides then build up in the upper bay, causing severe erosion, along the western shore and lower Mobile delta, and water and waves periodically cover the causeway across the lower Mobile delta.. These variations in water level cause complex currents that complicate the normal circulation within the bay. Somewhat the same situation exists in Perdido Bay, although the effects are not as pronounced because of its smaller size. 69 WIND FREQUENCY DISTRIBUTION 19% 14% 9% 7% 'JANUARY RY 7% 14% 10% 8% 6% 8% 15% JULY 12% 14% 14% Position: 30'14' North latitude 880021 West longitude. 0 30 Percent Percent of month that winds ore from a given octant. Figure 29. --Wind roses for coastal Alabama, January and July. 70 Severe Weather Disturbances The coastal area of Alabama has experienced the effects of 24 tropical storms or hurricanes between 1901 and 1955. Simpson and Laurence (1971) predict that in an 80-km (50-mi.) segment of coastline between Biloxi, Missis- pippi, and the mouth of Mobile Bay, the probability of landfall of a tropical storm is 13 percent, of a hurricane 6 percent, and of a great hurricane 1 percent for any one year. The aspects of such severe weather disturbances that cause the greatest changes to shorelines and near-shore bottoms are storm surges, waves, and cur- rents (Hayes, 1967). Storm surge, the rapid rise in sea level partially produced by hurricane winds and failing barometric pressure, may inundate vast areas of low-lying coastal areas, producing significant and wide spreaderosion and deposition of shoreline and near-shore sediments. Considering that a hurricane or tropical storm may last for several days, tremendous quantities of water can be amassed against the coastline (Hayes, 1967). Surges in Alabama have been recorded as high as 3. 60 m (11. 8 ft) above MLW and as low as 2. 96 m (9. 7 ft) below MLW. When a storm surge advances up a converging estuary such as Mobile Bay or Perdido Bay, its height increases as the water becomes more confined. The storm surge progresses more.rapidly on a rising tide and may result in the 71 formation of a wall-like wave of water moving up the estuary (Chermock, 1975.) There is a great danger of damage by hurricane storm surge along much Of the Alabama coastal area because many areas along Mississippi Sound, Dauphin Island, Morgan Peninsula, and the gulf shoreline are below 3. 0 m (10 ft) elevation In these areas, surge with destructive waves can remove vast quantities of sedi- ments; and destroy coastal structures. Because the effects of storm surge may be attenuated by the barrier dune complex along the gulf shoreline and the eastern end of Dauphin Island, the gulf beaches are the areas most subject to surf erosion. Probably the most significant effect of hurricanes is the erosion produced by break- ing *aves. Large waves riding the crest of a large storm surge can cause great devastation especially to cliffed or dunal shorelines. Breaking waves also can generate strong longshore and rip currents which may remove sedirnents from the shore and near-shore areas (Hayes, 1967). During severe weather disturbances, -extremely rough sea conditions pro- hibit the use of surface ships for taking oceanographic measurements (Hayes, 19 67 and high winds and rainfall make the use of current meters extremely hazardous. So, little is known about the currents generated under such conditions other than the obvious: they must be very strong. 72 Sediment Budget Variations The sediment budget for the coastal system is the net amount of sediment in the coastal area after considering the quantity of material being introduced, the quantity temporarily stored (dunes) and the quantity being removed from the coastal system. Beaches are nourished and maintained by gand-size sediment contributed by major streams, updrift shoreline erosion, onshore movement of shelf sand by wave action (Brown, and others, 1974) and by current circulation. Sand losses are cau sed by transportation offshore into deep water, accretion alongand against natural barriers and man-made structures, deposition in tidal deltas and hurricane washover fans, excavation for proposed construction, and eolian processes (Brown, and others, 1974). Sediment is supplied to the coastal area by the Mobile River system and by the Perdido River system. Ryan (1969) estimates that the suspended sediment load reaching Mobile delta and bay averages 4. 3 million metric tons (4. 7 million tons) per year and ranges from 1. 9 million metric tons to 7. 5 million metric tons (2. 1 million tons to 8.3 million tons) per year. Of the 4.3 million metric tons per year introduced, an estimated 1. 3 million metric tons (1. 4 million tons) per year, or 30 percent of the total introduced, passes through the estuarine system to the gulf. No quantitative data on bed load transported by the Mobile River system is available. 73 Similar data are not now available for Perdido River flowing into Perdido Bay (Boone, 1973). Prevailing south and southeast winds generate waves that produce a west- ward-flowing current along the gulf shore. A net longshore drift of 49,699 m3 (65, 000 yd3) per year at Perdido Pass has been reported to enter the Alabama coastal area. D. S. Gorsline, using wave-energy equations, calculated the net drift at Gulf Shores at 149,853 m3 (196, 000 yd3) per year. This drift continues to the mouth of Mobile Bay, a major drift barrier, where much of the material is carried offshore. Drift volumes within the bays have never been estimated but are probably small (U.S. Army Corps of Engineers, 1973). These examples give only brief glimpses of a complex sedimentary budget. Obviously, much work needs to be done on the variations in movement and the fate of sediments within the coastal system of Alabama. Sea Level Changes Shoreline changes caused by variations in sea level are termed eustatic. Eustatic changes can arise through diastrophism, which is connected with changes in the form ordepth of the ocean (Guilcher, 1954) or climatic changes, which cause variations in the volume of the continental ice sheets. 74 The National Ocean Survey has established 16 control tide stations along the gulf coast to continuously monitor tidal height and, during a period of at least 19 years, to determine changes taking place in the relative elevations of land and sea (Shalowitz, 1964). None of these stations is located in Alabama. Tide-gage data gathered over the past 50 years along the Florida gulf coast show that there has been a relative subsidence of 0. 1 mm (0. 04 in) per year. This measurement is obviously composed of sea-4evel changes as well as land-4evel changes (Lazarus, 1965). However, Lazarus attributes most of this change to land subsidence and assigns a value of 0. 1 mm per year for the gulf coast from the mouth of the Mis- sissippi River to Key West. Based upon the superimposition of this local subsid- ence rate on the oscillations of sea level on a worldwide basis as these varied with time. Lazarus (1965) determined that sea level rose rapidly from -112 m (-368 ft) MSL about 18, 000 years before the present (B. P.) to -3.2 M (-10 ft) MSL about 5,800 years B. P. The rise in sea level slowed appreciably between 5, 800 years B. P. and the present time, rising in an errat ic manner in response to glacial cycle until the present stand was reached (Lazarus, 1965). Tidal gage records over the past few decades show evidence that changes in the relative levels of land and sea are still in progress (Bird, 1-969). On a low- lying coast such as that bordering much of the coastal area, a continuing relative rise in sea level will have a marked effect on the configuration of the shoreline. 75 DETAILED ASSESSMENT OF SHORELINE AND BATHYMETRIC CHANGES Histor ical shoreline and bathymetric change assessment shows that the co ast alshorelin e of Alabama is being significantly modified by winds, currents, and tides. Most of the coastal shoreline shows either a net accretion or a net erosion. A very few areas exhibit a state of equilibrium in shoreline movement over th e measured time interval. Since shoreline erosion is of primary concern, a map of shorelines show- ing a net erosional trend during the period of measurement was prepared (pl. 1). The trends shown on plate 1 represent the net changes between 1917 and 1956-74. Short-term changes caused by hurricanes, tropical storms, excessive winds, abnormally high tides, although important, obviously cannot be shown on this map. Measurements made by opisometer during the compilation of this map show that of a total of 8,11.4 km (503.9 mi.) of shoreline, 355. 7 km (220.9 mi.) showed. a net erosional trend, and 455. 7 km (283. 0 mi showed a net accre- tional trend, or a net state of equilibrium as determined by the methods of this study, Some caution is advised in the use of the figures because the limitations of -the method, as mentioned previously, do not allow for accurate measurements of small net changes. 76 Some areas are undergoing more rapid erosion or accretion and must be analyzed and described in more detail. For this study, the shoreline has been divided into nine regions: 1) the Mobile delta, 2) Mobile harbor, 3) the western shore, 4) Mississippi Sound, north shore, 5) Dauphin Island, 6) the eastern shore 7) Morgan Peninsula, bay shore, 8) the gulf shore, and 9) Perdido Bay. These regions are shown on plate 1. The areas of erosion, accretion or shoreline stability will be emphasized, along with consideration of the possible causes. Mobile Delta The Mobile delta is a depositional feature that began filling the Alabama River estuary some 3, 000 years ago (Russell, 1967). This prograding delta has filled over 64 km (40 mi.) of the original estuary. Most of the delta has remained'in a near-natural state with the exceptions of the lower terminus, where much land filling and causeway construction (1927) has occurred, and on Blakeley and Pinto Islands where much landfill and industrial /commercial expansion has taken place. In the analysis of shoreline changes, the Mobile delta was divided into two regions, one being that part of the delta least subject to alterations by man, desig- nated as the Mobile delta region, and the other being that area most subject to the 77 constructions of man, the Mobile harbor region. Although some mingling occurs, this division was established to facilitate the differentiation of changes in shore- line caused by natural processes from those changes due to man's activities. Between 1917 and 1967, the shoreline of the Mobile delta has shown a small net erosional trend even though a few areas exhibit a state of equilibrium. Erosion has occurred principally along the channel margins of distributary rivers such as the western bank of the Blakeley River, the eastern bank of the Apalachee River, and along areas of both banks of the Tensaw River and Spanish River (figs. 30 and 31). Most of the accretion has occurred within the inter distributary bays and along the remaining banks of the distributaries. The tips of the natural levees marginal to the distributaries show both erosion and accretion. Figure 32 shows graphically the rates of accretion at the tip of the western natural levee of the Apalachee River. Between 1953 and 1967, there was a distinct erosional trend in all the inter distributary bays which reverses the accretional trend of the past 36 years. Between 1917 and 1967, net change of minus 8. 92 ha (22. 04 a.) of area oc- curred in the Mobile delta. In an environment where increased sediment deposition and land-building should occur, a large net addition should be expected. That such an accretion did not occur indicates that the delta's progradation has decelerated. Such a situation might be partly caused by a decrease in sediment being trans- ported downstream by the Mobile River as a result of upstream impoundments, 78 8r57' 30" C4 CD TI m ..... 0 f Chocoloochee Bay t BaY Minette 14 0 m A MOBILE BAY 0 Shoreline 1917 Mile - - - - Shoreline 1953 a, 0 MOBILE DELTA 1917-1953 8r57'301, F igure 30. --Shoreline changes in the Mobile delta region, 1917-1953. 79 8r57'30" C@ 0, Al Chocaloochee Ba Bay Minette X Cc so a 713 w < MOBILE BAY xp @o 16 12 OA ell mi Shoreline 1953 Shoreline 1967 CP MOBILE DELTA, 1953-1967 8r57'30" Figure 31. --Shoreline change in the Mobile delta region, 1953-1967. 1000 N 3000 0 z -n iM 2000 m >r --1 500 M M 1000 > z n 1917 1920 1930 1940 1950 1960 1967 M 00 Figure 32. --Changes in the rate of accretion for various time periods at the tip of the western natural levee of the Apalachee River, 1917-1967. 81 or by short periods of high discharge (floods). The greatly increased velocity of water flowing over the delta during such floods could cause much erosion in a short period. Mobile Harbor The region designated Mobile harbor lies between 3003713011 and 3004410011 north latitude and between 88'0410011 and 88'0410011 west longitude (pl. 1). The most significant characteristic of the Mobile harbor area is the ex- tensive accretion of shoreline caused by the continued spoils disposal and landfill carried out in the development of the harbor and the adjacent industrial /commer- cial complex. Table 5 shows the actual areas of landfill at various intervals since 1917. Some 668.31 ha (1, 650. 73 a.) of land was made by the combined efforts of spoils disposal and landfill in the area shown in figure 33. Table 5. --Area of landfill, Mobile harbor, 1917 to 1974, in hectares (acres) Period Area built up 1917-1940 86. 62 ha (213.95 a.) 1940-1953 80. 99 ha (200. 04 a.) 1953-1967 274.95 ha (679. 14 a.) 1967-1974 225. 75 ha (557. 60 a.) Total 668. 75 ha (1,650. 73 a.) 82 Many other coastal areas have been filled, but not at a rate as rapid as that in the Mobile harbor region. Crance (1971) reported a total of 871 ha (2,152 a.) of estuary filled above MLW in Alabama between 1953 and 1971. The total is subdivided into various areas of coastal Alabama, as shown in table 6. Figures 33 and 34 show the areas of accretion in Mobile harbor between various time periods from 1917 to 1974. Most of this "made-land" occurs on Blakeley Island, Pinto Island, McDuffie Island, and Little Sand Island. Figure 35 shows the rate of construction of made land during various periods between 1917 and 1974. The highest rate concurs with the period of rapid development in Mobile during the 1950's and 19601s. Western Shore Ihe western shore of Mobile Bay begins, for the purposes of this study, at the Brookley Aerospace Complex and continues down the entire western shore of Mobile Bay to Cedar Point. Three major tidal creeks, Dog River, Deer River, and Fowl River, enter the bay on the western shore. The shoreline consists of a narrow sandy or marshy shoreline backed mostly by actively eroding seacliffs ranging from 1. 5 to 4. 6 km (5 to 15 ft) high as far south as Alabama Port. Trees felled by the constant erosion may be seen along almost the entire shoreline. mom m mm m m1m m m mm m mm, m m m m Table 6. --Filled areas in the Alabama estuaries Emergent Housing, spoil industry or Area banks (MLW) Causeways other uses Total. Mississippi Sound 34. 6 ha (85 a.) Graveline, Aloe and 0. 8 ha (2 a.) 0.8 ha (2 a.) 16. 2 ha (40 a.) Dauphin Island Bays Dauphin Island Airport 0.4 ha (1 a.) 14. 2 ha (3 5 a.) Miscellaneous 2.0 ha (5 a.) 00 Mobile Bay 347. 2 ha (858 a.) Brookley Field extension 83. 4 ha (206 a.) McDuffie Island area 5. 6 ha (14 a.) 1. 2 ha (3 a.) 93. 1 ha (230 a.) Battleship Park 73.2 ha (181 a.) Meaher Park 35. 6 ha (88 a.) Pinto Island 12.1 ha (30 a.) Little Sand Island area 14. 5 ha (36 a.) Miscellaneous 14. 2 ha (3 5 a.) 14.2 ha (35 a.) Mobile Delta 484. 0 ha (1,119 a.) Polecat Bay 405. 5 ha (1,002 a.) Sardine Pass 50.2 ha (124 a.) Miscellaneous 14. 2 ha (35 a.) 14. 2 ha (35 a.) Perdido Bay 0. 4 ha (1 a.) 4. 0 ha (10 a.) 4. 4 ha (11 a.) Little Lagoon 0.8 ha (2 a.) 0. 8 ha (2 a. Total 6. 8 ha (17 a.) 30. 8 ha (76 a..) 833.3 ha (2,059 a.) 870. 9 ha (2,152 a.) LO ol U- 0 LL 0 0 ol BLAKELEY ISLA D u 0 C.)- - ------ < 00 LU co 0 30P 42' 30" 30' 401 00 Ll 01 0 LU 0% lpo LL U- :3 0% oc, Q oky BLAKELEY ISLAND u 0 CD tMAO 13L CV IJ CD co 30P 421 30" 300 40' BLAKELEY ISLAND 10 TI u 0 co R m v @o E Go uj ca 0 :E 300 42' 30" 300 of LO I O'll 10 cl) LO LL oly BLAKELEY iSLAND 0 CID R < E CO LLJ 00 0 300 42' 30" 30 40' ,u 0 If co III @Alr) uj 0 30-401 kBLAKELEI 2000 . 4000 0 1000 LO M - 3000 N -1 0 M _n z ;0 --1 - 2000 M > 500 M 1000 > 00 0 0 z n 1917 20 1930 1940 1950 53 1960 67 1970 74 M Figure 35. --Changes in the rate of landfill for various time periods at McDuffie Island, 1917-1974. 87 All along the western shore of Mobile Bay south from Brookley Aerospace Complex to Cedar Point there has occurred a persistent and significant erosional trend of from less than 1. 52 m (5 ft) per year in most areas to as much as 2. 60 m (8. 56 ft) per year and averagin g 0. 97 m (3. 17 ft) per year at Cedar Point based on various intervals of time. Table 7 shows measurements made of the shoreline changes at points identifiable on U. S. Geological Survey 7. 5-minute topographic sheets. As this table shows, erosion at measured points has ranged from 12 m (39 ft) at Pt. Judith to 149 m (488 ft) at Cedar Point during 1917-1974. The areas between Dog River Point and Fowl River Point and between Delchamps Bayou and Cedar Point show the most severe amounts of erosion (pl. 1). Figure 36 shows the shoreline changes between Dog River Bridge and Fowl River Point during various time periods between 1917 and 1967. The persistent and severe erosion shown in this area is broken only by accretion caused by spoils disposal in an area north of the Hollingers Island Channel (proposed Theodore Ship Channel). Erosion in the area is threatening waterfront residents throughout the area. The severe erosion along the shore between Alabama Port and Cedar Point has already partly destroyed a railroad right-of-way to the east of Highway 163. Erosion is now threatening the highway itself at some points. The Cedar Point 88 Table 7. --Shoreline changes measured at selected identifiable points along the western shore of Mobile Bay. Location Change Time period Average annual change 1. Dog River Point (at bench -83. 8m 1917-1967 1. 68m mark) (-275 ft) (5.51 ft) 2. Mobile Yacht Club (at pier) -120. 1m 1917-1967 2.40m (-394 ft) (7. 87 ft) 3. Deer River Point (at new -47. 9m 1917-1967 0. 96m pier) (-157 ft) (3. 15 ft) 4. Bellefontaine (at name on -36. Orn 1917-1958 0. 88M map) (-118 ft) (2. 88 ft) 5. Sunny Cove (at name) -52..7m 1917-1958 1. 29m (-173 ft) (4. 23 ft) 6. Fowl River Point (at bench -4 3. 3m 1917-1958 1. 05m mark) (-142 ft) (3.46 ft) 7. Mon Louis (at name) -24. Im 1917-1958 0. 59m (- 79 ft) (1. 93 ft) 8. Faustinas (at name) -29.9m 1917-1958 0. 73m 98 ft) (2.40 ft) 9. Pt. Judith (at name) -11. 9m 1917-1974 0. 20m (- 39 ft) (0. 68 ft) 10. Alabama Port (at name) -43. 3m 1917-1974 0. 76m (-142 ft) (2.49 ft) 11. Cedar Point (at30*20100"N. -107.9m 1917-1974 1. 90M latitude (-354 ft) @(6.22 ft) 12. Cedar Point (at Hwy 163 -148.7m 1917-1974 2.61m symbol) (-488 ft) (8.56 ft) *Positive changes show accretion; negative changes show erosion. 89 Dog River Bridge 8005, ................ DOG RIVER BRIDGE TO DEER RIVER TO FOWL RIVER DEER RIVER, 1917 TO 1967 POINT, 1917 TO 1956, 1967 i::": i M i: .......... 7 7 Mobile Co. 30030' INGERS ISLAN Bellqfontaine 3 iver .......... . ... .. ........ ..... Sunny Cove Theodore1nd .............. ...... . . . . . . . . . . . ... ... ....... Hollingers Island Shoreline 1917 Ship Channel Shoreline 1940 N 9Y . ... ...... 0 2000 Feet ........ ... Figure 36. --Shoreline 'Changes between Dog River Bridge and Fowl River Point between 1917 and 1967. 90 area is very important to the continued protection of the salt marshes of southern Hollingers Island in Mississippi Sound from the full effects of winds, waves, and currents from Mobile Bay. The southern tip of Cedar Point has persistently shown one of the highest rates of erosion recorded for the coastal area. Between 1917 and 1974, 149 m (488 ft) of erosion has been measured (table 7). The change in rate of erosion for various time periods is shown in figure 37. Mississippi Sound, North Shore The northern shoreline of Mississippi Sound is mostly made up of low-lying salt marsh with numerous tidal creeks, the principal ones being West Fowl River, Bayou Coden, and Bayou La Batre. The shoreline of Mississippi Sound, including the barrier islands to the south, totals 201 km (125 mi.), excluding the length of tidal streams, of which 162 km (101 mi.) consist of tidal marsh (Crance, 1971). Most of the region's 4, 762 ha (11, 762 a.) (Crance, 1971) of tidal marsh is found around Grand Bay, Fowl River Bay, Heron Bay, and on the numerous small is- lands in the Sound. With the exception of residential and commercial fisheries development in the princ ipal tidal creeks, most of the northern shoreline remains in a natural state. The southern shoreline of Mississippi Sound is comprised of sandy barrier islands that protect the northern marshy coast from the full impact of erosional agents. These islands will be discussed more fully in a later section. 91 horizontal distance feet C> C> C) C) C> C) C) C@ C) C> C) N CO LO C) 0 m P, (M @4 Ca 0 Cq 0 C> '"0 bD 92 Between 1917 and 1958, most of the northern shoreline of Mississippi Sound experienced net shoreline erosion. The amount of erosion measured at selected points identifiable on U.S. Geological Survey 7. 5-minute topographic maps of the area varied between 47. 85 m (157 ft) on Marsh Island (Grand Bay) and 132. 28 m (434 ft) on Marsh Island (Portersville Bay) as shown on table 8. These represent erosional trends ranging from 1. 1 7 m (3. 84 ft) per year to 3. 7 7 m (10. 56 ft) per year for those specific points. The changes in the rate of erosion for selected points over various time periods are shown in figure 38. The generalized areas of erosion in Mississippi Sound are shown on plate 1. Most of the erosion of Mississippi Sound has occurred on exposed marshy head- lands and on exposed shorelines at the numerous islands. Cat Island lost an average of 59. 89 m (19 6. 5 ft) of its southern shore, and Isle aux Herbes lost an average of 99. 06 m (325. 0 ft) of its southwestern shore between 1917 and 1958 (table 9). It is estimated that many exposed shorelines of Mississippi Sound are eroding at an average rate of 1 to 2 m (3. 28 to 6. 56 ft) per year, on the basis of measure- ments made at selected points and average rates measured. Dauphin Island Area Dauphin Island is part of a chain of barrier islands protecting Mississippi Sound from erosional forces from the Gulf of Mexico. These islands absorb almost the full 93 Table 8. --Shoreline changes measured at selected identifiable points along the northern shore of Mississippi Sound Average annual Location Change* Time period erosion 1. Barron Point -96. 0 m 1917-1955 2.34 m (-315 ft) (7. 68 ft) 2. Cat Island (southeast shore) -101 m 1917-1958 2.46 m (-331 ft) 1 (8. 07 ft) 3. Marsh Island (southeast shore) -132 m 1917-1958 3.77 m (Portersville Bay) (-434 ft) (10. 56 ft) 4. Isle aux Herbes (eastern shore) -71.9 m 1917-1958 1. 76 m (-236 ft) (5. 76 ft) 5. Isle aux Dames (88'18100" W. -81. 1 m 1917-1958 2.05 m longitude (-276 ft) (6. 72 ft) 6. Point aux Pins (at range line) -7.1.9 m 1917-1958 1. 75 m (-236 ft) (5. 76 ft) 7. Marsh Island (mid-island) -47.9 m 1917-1958 1. 17 m (Grand Bay) (-157 ft) (3. 84 ft) 8. Grand Batture Islands (South -120 m 1917-1958 2.93 m Rigolets Island, 1, 000 m east (-393 ft) (9. 60 ft) of state line) Positive changes show accretion; negative changes show erosion. 94 0 0 N U) r+ 100, -300 m CL E 91 1917 1941 1 58 0 Point aux Pins 0 :2 N 0 0 m 100- -600 E -200 0 1917 19,41 19,58 Isle aux Herbes 0 N 0 0 m -100 CD 75 E 9' _j 0 1917 1 41 1958 1974 CD West side of Cedar Point 0 0 0 N 0 W " -100- -300 m 4) -601D E 200 r+ 2) -900 1917 1941 19,58 m West side of Marsh Island Figure 38. --Changes in the rate of erosion at selected points along the northern shore of the Mississippi Sound. Table 9. --Changes in area and average erosion rates for selected areas in Mississippi Sound Location Area in 1917 Area in 1958 Change in area Average erosion Average annual erosion 1. Barron Point to Barry 45.72 m (1) 1. 12 m Point area (150. 0 ft) (3. 66 ft) 2. Cat Island 9. 29 ha 9. 29 ha 0 59. 89 m (1) 1.46 m (22. 96 a) (22.96 a) (196.5 ft) (4.79 ft) 3. Marsh Island 36. 06 ha 27. 14 ha -8.92 ha 87.08 m (1) 2.12 m (Portersville Bay) (89. 02 a) (67. 03 a) (-22.4 a) (285. 7 ft) (6.97 ft) 4. Isle aux Herbes 314. 15 ha 267. 30 ha -46. 85 ha 99. 06 m (2) 2.42 m CD (7 7 5. 94 a) (6 6 0. 24 a) (-115.7 a) (325. 0 ft) (7.93 ft) 41.76 m (3) 1. 02 m (137.0 ft) (3.34 ft) 5. Point aux Pins - - -9. 67 ha 79.25 m (1) 1.93 m (-23. 87 a) (260 ft) (6.34 ft) (1) Shore having southern exposure (2) Shore having southwestern exposure (3) Shore having eastern exposure 96 impact of winds, wave action, tides, and currents; and their configuration is constantly changing. Dauphin Island is 24. 35 km (15. 13. mi.) long and varies from 305-549 m (1, 000-1, 800 ft) wide across the western sandy spit to 2. 6 km (1. 6 mi.) wide across the forested main body of the island near the eastern end. Elevations at the east end of the island are generally between 1. 5 and 3 m (5 and,10 ft), except- ing a large east-west trending dune system as much as 14 m (45 ft) above mean sea level. Most of the population of Dauphin Island is concentrated in the eastern 11 km (7 mi.) of the island, either along the bay margins of the main body of the island or along the first 5 or 6 km (3 or 4 mi.) of the spit, where much new resi- dential development has occurred. The shorelines of Dauphin Island have been greatly modified throughout its known history. Shortly after 1717, a Frenchman, Sr Du Sault, produced a map of the island that indicated strongly that at that date, Dauphin Island and Petit Bois Island, presently immediately west of Dauphin Island, were connected. At some later date the island was breached. This conclusion was reached because the "Isle Dauphine" shown on the circa 1717 map has a hump on the western spit very similar to the hump of the present day Petit Bois Island. Also, the next island to the west on the circa 1717 map was called "Isle a Cornell, Horn Island, which is the island to the west of the present day Petit Bois Island. 97 Between 1909 and 1917 a hurricane breached Dauphin Island, dividing it into two smaller islands separated by 8. 5 km (5.3 mi.) of open water, shoals, and scattered remnants of the former island. The western island was 6. 1 km (3. 8 mi.) long and the eastern island was 6. 7 km (4. 2 mi..) long (fig. 39) Between 1917 and 1942, the hurricane- created tidal inlet filled with sediment, thus rejoining the two islands to form one island. Air photos taken on March 23, 1950, show Dauphin Island again breached by the hurricane of September 4 , 1948. Tides generated by this hurricane were reported to be 1. 8 m (6 ft) above normal at Coden and Bayou La Batre (U. S. Army Corps of Engineers, 1973). The island was breached about 1, 219 m (4, 000 ft) west of Oro Point. The breached area was approximately 42 7 m (1, 400 ft) wide and, by the date of the photos, was probably covered only at high tide. A washover fan extended over much of the length of the island but was best developed for a distance of 3. 2 km (2 mi.) west of Bayou Heron channel. Extensive residential development has occurred in this area since 1950 (fig. 40). Because this area has been breached twice by hurricanes in this century, there is every reason to believe that it will again be breached, at great cost to private prop- erty in the area. Paradoxically, most of the new residential developm ent has DAUPHIN ISLAND 1917-1942 88010' 88005, 4fo Mississippi SOUND 40 Pass Drury '94), AUPHIN 30'15 - ------F ---------- ----------------------------------- --------- GULF A MATCH LINE 88010, 88015' 88005' 30015' 30 00 A MATCH LINE ... ... .... Land area 1917 K. Shoreline 1942 0 1 Leading edge of dune 191 Mile 88015' Leading edge of dune 194 FIgure 39. --Areas of shoreline changes at Dauphin Island between 1917 and 1942. 1950 UNOCCUPI . .. . .. .- "Me M % 1-tl 0 AT, 1975 DWELLING UNI 0 (D r C, C) 'iM Or ZM 100 occurred in areas most susceptible to storm damage, while large tracts of sub- divided land in the eastern part of the island protected by the large primary. dunal complex and a forest of pines are relatively undeveloped. The barrier dune complex slowly migrated north as much as 156 m (513 ft) between 1917 and 1942, forming a precipitation ridge where it is slowed or halted by the forest edge (fig. 39). No measurable movement was detected between 1942 and 1958 (fig. 41). Movements shown on figure 41 are attributed to differences in mapping techniques. Figure 41 shows a general trend of erosion along the gulf shore of the island and general elongation along the western end of the island. Figure 42 shows the rate of erosion for various time periods at locations along the gulf shore of the island. Shoreline erosion on the part of the island that was westernmost in 1917 (fig. 43) averaged 176. 0 m (577. 5 ft) over the period 1917 to 1974 or 3. 09 m (10. 13 ft) per year. The maximum measured erosion was 201. 2 m (660 ft), an average of 3. 53 m (11. 58 ft) per year for the period 1917 to 1974. Shoreline erosion on the entire gulf shore for the period 1942 to 1974 averaged 63. 70 m (209 ft) or 1. 93 m (6. 34 ft) per year excluding the accretion on the western tip of the island. This accretion has added a total of 2.9 km (1. 8 mi.) to the length of Dauphin Island from 1917 to 1974. DAUPHIN ISLAND, 1942-1974 88010, 880 410 MISSISSIPPI SOUND Pass ps, ---------- D A U P H I N ISLAND 3@00 151 ............ . ...... . . .... GULF OF A MATCH Ll NE C*0 88010' 88015' 880 30015' . .......... MATCH Ll Land area 1942 Shoreline 1974 Leading edge of dune, 1 Mile 88015' Leading edg .e of d.une 1 9 Figure 41. --Areas of shoreline changes at Dauphin Island between 1942 and 1974. -200 - - -600 -150 - - -500 - -400 M __q -100 M -300 M C/) - -200 -50 - -100 0 0 M 1920 1930 1942 1950 1958 1970 N 0 z -700 -200 -600 -500 -150 -400 -100 -300 -200 -50 -100 0 0 1920 1930 1942 1950 1958 1970 Figure 42. --Changes in the rates of erosion for various time periods for Bienville Beach, Dauphin Isla (88*071 W.) (upper graph) and west-central Dauphin Island (lower graph). M M M M M M M M M M M MMMM 4000 - 1200 3000 - 900 0 ;0 N 0 z m -4 __1 > m 2000 600 z n m 1000 300 1917 1930 1942 1950 1958 1970 1974 Figure 43. --Rate of accretion for the Nvestorn tip of Dauphin Island. 104 The accretion measured at the western tip of the island for various intervals of time is shown in table 10. Because of the different orientations of the longest axis of change, the amounts for the various time periods do not equal the total for the period of measurement. Table 10. --Amount of accretion at the western tip of Dauphin Island, 1917- 1974. 1917-1942 1, 270 m (4, 166 ft) 1942-1958 635 m (2,083 ft) 1958-1974 1, 429 m (4, 687 ft) 1917-1974 2,730 m (8,957 ft) The bathymetry of the Mobile Bay entrance and the passes associated with Little Dauphin Island is heavily influenced by dredging and associated spoil accu- mulation. The Mobile Ship Channel and Pass aux Herons (Pass Heron) are both dredged regularly, and the spoil from this is added to the sedimentalogical regime of the bay entrance. The areas adjacent to the main entrance are filling, and the relief of the gulf bottom is becoming flatter (figs. 44, 45, 46, and 47). Passes that are not regularly dredged are closing or have closed, such as Big Pass Mar- garet, Little Pass Margaret, Bayou Matagua, and Pass Drury (Gazzier, 1972). CED4R POINT .............. Land area Subaerial tidal MOBILE -15 It LZ 1--l Shoal areas I i PASS AUX HERONS /I 111Z ontour interva LC It BAY Scale 1: 106,60 Big Pass Morgaref it I LQ -.LITTLE D@UPHIN ISLAND 20 1 0 SS DRURY LITTLE POINT .. . ..... .. .4 300 15' D A U P S, N D MOBILE BAY TIDAL PASS PELICAN ISLAN d@ .. MOBILE POINT::- %0 "$P A; _50 -30010, /'---Dt.- -,.a. 10 88 88000, Figure 44. --Bathymetric contours, Mobile Bay entrance and associated -passes, 1929 (data from USCGS 1266, 1929). CEDAR POINT Land area if MOBILE Subaerial tidal flat PASS AUX HERONS if ,--I Shoal areas it j3 Contour interval 5 f Big Pass Margaret I/ Iq BAY Scale 1: 105,000 -U) Bayou Matagua L 00 ITTLE DAUPHIN ISLAND 0 .............. V` A SDRURY LITTLE POINT CL It % . . . . .. . . . . ............ .',"'DAUPHIN Q IS .......... . . . . . MOBILE BAY .......... COO TIDAL PA@S MORGAN .......... ................ . ..... ...... . :@MOBILE POINI SAND/PELICAN ISL N @@ @Vl lip 300 10'- 88005 88000' Datum mean f V 7, if @owou' inle 'v' Sc le 1: '05,0 Z@@J- r- Figure 45. Bathymetric contours, Mobile Bay and associated passes, 1941 (data from USCGS chart 1266, 1941). M so M CEDAR POINT If MOBILE If Land area 1:00 If Su6oerial tidal fl PASS AUX HERONS If Shoo I areas EJ4 BAY Contour interval Pass Margaret If 7 Scale 1: 105,000 Bayou Motagua, LP N11 LITTLE DAUPHIN ISLAND 0 PASS DRUR@ LITTLE POI T 1S, 1L)AUPHN %6 '10 -4 Xx .1 Icy, . ... . ..... .............. ....... . . . . ..................... BAY mur_ MOBILE PELICAN ISLAND TIDAL PA@S JAOBILE POINT -410 13, SAND ISLAND- 1P n @mc '170 30010, 88005@1 8.,00, Datum me Figure 46. --Bathymetric contours, Mobile Bay entrance and.a,ssociated passes, 1961 (datafrom USCGS 872, 1962). 1 DAR POINT -V-@-'C E D@ Land area Su6aerial tidal flat MOBILE PASS AUX HERONS Shoolareas it --g Z Contour interval 5 f Q) BAY Scale 1: 105,000 It L.U It :zz! -7 It TTLE DAUPHIN ISLAND OINT .......... . LITTLE P ......... @th PASS DRURY'-- ............ 015 D,,:.UPH ISLAND" zo M 'E BAY w OBII TIDAL PASS E \.j E Pol MOBI SAND PELICAN ISLA 140 96 -461 300 101@-@ a I // I Datum mean lo 88'65'\ 8801001@ GIN -- ----- Figure 47. --Bathymetric contours, Mobile Bay entrance and associated passes, 19 73 (data from USCGS ch 1266, 1973). 109 Pass Drury has been replaced by an artificial channel between Little Dauphin and Dauphin Island, parallel to the long axis of Little Dauphin (fig. 47). Sev- eral areas of drifting sandbanks have formed near Peavy Island and in Dauphin Island Bay (Gazzier, 1972, p. 38). The bathymetric contours for 1929 (fig. 44) show a depression with depths of more than 6 m (20 ft) south of the east end of Dauphin Island. By 1973, this depression accumulated an average of 1. 22 m (4 ft) of sediment in its deepest part between 1929 and 1973 (fig. 47). Southwest of the Mobile Bay entrance is Sand/Pelican Island, anemergent bar of an ebb-tidal delta. The bar is in a dynamic state and its shape, size, and location have changed continuously throughout historic times. It is especially affected by severe weather disturbance. The bar increased steadily from 1929 to 1973 and the present island is approximately 2. 74 km (1. 70 mi..) long and sup- ports vegetation on the southeast end (fig. 48). East of Sand/Pelican Island adjacent to the Mobile Ship Channel is a small, intermittently subaerial bar called Sand Island on the Fort Morgan 7-g-minute quadrangle map of 1958. This is probably a channel-margin bar (Hayes and others, 1973). 110 Z-0 Figure 48. --Sand/Pelican Island, 1975. Concurrent with the accretionary trend of the western tip of Dauphin Island there has been a pronounced change in the configuration of Petit Bois Pass, which separates Dauphin Island and Petit Bois Island. As previously mentioned, circa 1717, the pass probably was not in existence. The earliest coastal survey avail- able, the survey of 1848, shows the pass to be well developed. The width of Petit Bois Pass has varied from 2. 61 km (1. 62 mi.) in 1848 to 7. 51 km (4. 66 mi.) in 1974 (table 11). During this same interval the pass migrated 12.40 km (7.71mi.) Table 11. --Width and westward migration of Petit Bois Pass at various time periods between 1848 and 1974 Year Width Westward migration* 1848 2. 61 km (1. 62 mi.) 1917 6.52 km (4.05 mi.) 8.57 km (5.32 mi.) 1848-1917 1942 7.65 km (4.75 mi.) 2. 61 km (1. 62 mi.) 1917-1942 1958 8.48 km (5.27 mi.) 1. 31 km (0. 81 mi.) 1942-1958 1974 7.51 km (4.66.mi.) Imperceptible 1958-1974 Total 12.40 km (7.71 mi.) 1848-1974 *Westward migration was measured by calculating the westward movement of the eastern tip of Petit Bois Island. westward. Figures 49 and 50 illustrate the changes in the configuration of Petit Bois Pass between 1848 and 1974. The widening of the pass and its westward migration are clearly shown. However, not only has the pass been modified in width and location, but also changes in the configuration of the bottom have oc- curred. Between 1917 and 1933, very little apparent change in the bottom config- uration of the pass occurred. This lack of change may have been due to slight stabilization of coastal erosion and accretion during this period, or may merely reflect use of older sounding data on the 1933 edition of the charts (fig. 51). PETIT BOIS PASS 1848-1917 88020' 300 88025' Co PETIT BOIS PASS 7, 7:X1 P E T I T B 0 1 SISLAND.-.. Land area in 1848 Shoreline 1917 88"25' 88020' 88D1 51 PETIT BOIS PASS 1917-1942 88D20' 00750. 880 25' C13 801 1 LAND Z7 PASS PETIT BOIS Land or,, in 1917 Shoreline 1942 0 MILE .880251 88020' 880 1301! Figure 49. --Changes in the configuration of PetitBois Pass between 1848and 1942. m m M, m IIIIIIIIIIIN m mm mow m m m m m m PETIT BOIS PASS 1942-1958 88020' 0", 5, 88025' 03 _j Z BOIS D A PASS IS AN PETIT BOIS (.,._w@Lcnd area in 1942 Shoreline 1958 880251 88020' 880151 PETIT BOIS PASS 1958-1974 88020' 0075, 880251 ca 19774 PASS BOIS PETIT ISL -Land area in 1958 Shoreline 1974 MILE 880251 88020' 88" 15' Figure 50. --Changes in the configuration of Petit Bois Pass between 1942 and 1974. 880251 880 201 Land area MISSISSIPPI SOUND Sb..,ial tidal flats or 6ars Shoal areas D UPI 19 ....... . .. 15 --------PETIT BOIS PASS 20 26 ID 50 PETI T BOIS PAS 300 15'- Contour interva 1 5 feet '10 Datum mean low w4ter MISSiSSIPir'l SOUND i Scale 1: 95,000 TEAUP04 PETIT BOIS PASS i@'. But:) P EX -I 8 25' 88 20' PETIT BOIS PAS )N P@ASS Figure 51. Bathymetric contours, Petit Bois Pass, 1917 and 1933 (data from USCGS charts 1267, 1917 and 1933). 115 The bathymetric map for 1961 shows several significant changes in the islands I shorelines; the western tip of Dauphin Island prograded, westward and the easternmost spit of Petit Bois Island apparently was eroded to such an extent that it was covered by the highest tides (fig. 52). The change in the configura- tion of the islands, however, did not affect the bottom configuration greatly. The tidal scour channel just west of Dauphin Island (at about longitude 880191), as de- lineated by a 20-foct contour line, became narrower and more elongate, but the basic configuration of the bottom changed little. By 1973, however, the eastern spit of Petit Bois Island had been eroded to below MLW, producing a wider outlet for the waters from Portersville Bay. This has reduced current velocities through the scour channel, and different patterns of sedimentation and erosion have been produced, The eastern end of Petit Bois Island has become a series of sand shoals in the pass, and an ebb- tidal bar (delineated by the closed 10-ft contour linefrom longitude 880191 to 880201) is beginning to form at the seaward end of the scour channel (fig. 52). If Petit Bois Pass is considered only as the area of open water between the western end of Dauphin Island and the eastern tip of Petit Bois Island, then the pass migrated westward along with the islands during the period from 1917 to 1973. However, it is significant that the scour channel, the deepest part of the pass, remained stationary during this period; even after 1961, when the 88025' 880201 Land area MISSISSIPPI SOUND Subaerial tidal flats or 6ars Shoal areas PETIT,B IS PASS AS .0 to 9. 96 -4.4 PETIT 130 30015' Contour interva 1 5 feet MISSISSIPPI SOUND Datum mean low water I Scale 1: 95,000 /Ar PETIT BOIS ASS '0 .... ... ... ... . .. 3S .......... ETIT! .... ....... . . . . . . . . . . 88025' 88020' PETIT 1301 Figure 52. Bathymetric contours, Petit Bois Pass, 1961 and 1973 (data from USCGS charts 873, 1 1267, 1973). 117 western tip of Dauphin Island had prograded across the northern end of the chan- nel, and should have deflected ebb-tidal currents and somewhat reduced their velocity, the channel remained in the same place and maintained its general depth. Only recently, since erosion of the eastern end of Petit Bois Island widened the pass significantly, has the scour channel become shallower and less well de- fined. This suggests that Petit Bois Pass channel has been "pinned" in place by some geologic factor or factors; possibly by the pre-Pleistocene channel of the Escatawpa River (P.A. Boone, personal communication, 1975). Eastern Shore The eastern shore of Mobi le Bay extends from D'Olive Bay about 2. 0 km (1. 24 mi..) south of Spanish Fort (13ridgehead) southward some 48 km (30 mi.) to the mouth of Bon Secour River. The shore from D'Olive Bay to Magnolia Beach south of Fairhope is generally a sandy beach backed by a sea cliff 3 to 33. 5 m (10 to 110 ft) high. South of Magnolia Beach, the shore consists of low- lying wetlands varying from less than 0. 5 km (0. 3 1 mi.) to more. than 1. 5 km (0. 93 mi.) wide. Most of the eastern shore has undergone accretion or has maintained a state of dynamic equilibrium between 1917 and 1967 or 197-4. The major shorelines of net accretion between 1917 and 1967 are the shore from Village Point south to Red Bluff, the shore south from Great Point Clear for 5. 1 km (3. 2 mi.), and the shore from Dorgans Landing at the mouth of Weeks Bay south to the mouth of Skunk Bayou just north of Weeks Bay. Erosion along the eastern shore occurs intermittently and is of less mag- nitude than in most other areas studied. However, some shorelines showing erosion are in highly desirable residential areas and thus could require expen- sive erosion-control construction. Erosion has occurred sporadically along the shore from Loyola Villa to Great Point Clear between 1917 and 1956-1967. Net' erosion of a shore just south of Loyola Villa was 60 m (197 ft) between 1917-1956 or 1. 5 m (5. 0 ft) per year. Other minor areas of erosion are Red Bluff, Seacliff, the area between Darling Landing and Mullet Point and several areas south of Mullet Point. Shore- line changes at various points identifiable on U.S. Geological Survey 7. 5-minute topographic maps are shown in table 12. Variations in the rate of shoreline change are shown for Village Point and an area south of Magnolia Beach in figure 53. 119 Table 12. --Shoreline changes measured at selected identifiable points along the eastern shore of Mobile Bay Location Change* Time period Annual rate Village Point +108 m 1917-1967 2. 16 m (+354 ft) (7. 08 ft) Red Bluff -36. 6 m 1917-1967 0. 73 m (- 12 0 ft) (2. 4 ft) Seacliff -12 m 1917-1967 0. 24 m (- 7 8 ft) (0. 78 ft) Fairhope municipal +60 m 1917-1967 1.2 m wharf (+197 ft) (3. 9 ft) Loyola Villa -60 m 1917-1956 1.5 m (-197 ft) (5. 0 ft) Great Point Clear +36 m 0. 92 m (+118 ft) (3. 0 ft) Point Clear +54 m 1.4 m (+177 ft) (4. 5 ft) Near Mullet Point -47. 9 m 1. 2 m Park 300251 N. lati- 15 7 ft) (4. 0 ft) tude Positive changes show accretion; negative changes show erosion. 400 0 100- -300 0 P -200 a) (D 4 2 50- 100 C+ 0 0 (D 1930 1941 1950 1960 1970 0 19120 19.30 19.41 19153 19160 19.70 0 P-ft C+ 100 CD CD 50- CIP, 200 W 100- Figure 53. --Rates of accretion at Village Point (upper graph) and erosion for an area south of Magnolia Beach (lower graph). 121 Morgan Peninsula, Bay Shore Morgan Peninsula is a large baymouth bar extending westward from the eastern shore of Mobile Bay. This peninsula, which varies from 0. 28 km (0. 46 mi.) to 3. 59 km (2. 23 mi.) wide and is 29. 0 km (18. 0 mi.) in length, separates the bay water from the gulf water, and insures the maintenance of an estuarine environment in Mobile Bay, and care should be exercised to insure its continued effectiveness as a protective barrier. Erosion, measurable along much of the northern shore and probably existing along almost the entire length of the shore from the mouth of Bon Secour River to Fort Morgan, is a major concern for resi- dents of the shore from Seymour Bluff to Catlins Bayou. Measurements of the change in shoreline configuration between 1917 and 1974 show that as much as 52 m (170 ft) of erosion may have occurred from the mouth of Bon Secour River to Catlins Bayou during that time. Although no measureable erosion was discerned between Catlins Bayou and Three Rivers during 1917-1942, shoreline erosion did occur between 1974 in the Edith Hammock area. Some areas showed as much as 30.5 m (100 ft) of erosion between 1942 and 1974, although the average amount was closer to 15. 3 m (50 ft). From Three Rivers to the eastern seawall of Fort Morgan, much erosion and shoreline modification has occurred. From Little Point Clear to St. Andrews Bay, termini of bayward-projecting ancient spits lost from 61 to 244 m (200 to 800 ft) 122 between 1617 and 1974. From Navy Cove to the eastern seawall of Fort Morgan, losses on the order of 61 m (200 ft) were noted. Examination of bathymetric data from 1929 to 1973 (figs. 44, 45, 46, and 47) reveals that St. Andrews Bay, Navy Cove, and the bay north of Fort Morgan are becoming progressively shallower. The southwest cove of St. Andrews Bay has also become a shoal area. This trend probably reflects deposition of material eroded from the shoreline west of Little Point Clear, as well as material from the spoil banks on the south side of the Intracoastal Waterway north of Morgan Penin- sula, and from the spoil banks northwest of the peninsula along the Mobile Ship Channel. A long underwater spit, known locally as Dixie Bar, extends about 5. 6 km (3.4 mi.) south into the gulf from Mobile Point. Between 1929 and 1973, this spit became somewhat more narrow and elongate, and the southern tip appears to have moved slightly west (figs. 44 and 47). This trend indicates little or no deposition on the spit, either because the longshore currents are strong enough to erode it, or that very little material is being eroded from the gulf shore of the peninsula to the east (fig. 47). 123 Gulf Shore The Gulf shore region of coastal Alabama extends from Mobile Point to the Florida state line and is some 50 km (31 mi.) in length. The shoreline of white sandy beaches is backed by low dunes. In 1917, several tidal inlets existed. These inlets opened into Little Lagoon and Shelby Lakes. The inlet connpcting Little Lagoon to the Gulf was 1. 1 km (0. 7 mi.) west of Gulf Shores beach. This inlet was approximately 80 km (262 ft) wide. A second inlet along the gulf shoreline was approximately 1. 7 km (1. 1 mi.) west of Romar Beach, as located on the Foley, Alabama, 15-minute U. S. Geological Survey topographic map. This inlet connected the easternmost. lagoon onthe Shelby Lakes with the gulf, and was approximately 20 km (66 ft) wide. By 1941, both of these inlets had closed and a second inlet to Little Lagoon had opened. This inlet, 3. 5 km (2. 2 mi.) west of the inlet of 1917, was about 60 m (197 ft) wide. High-altitude infrared photog- raphy taken in 1974 of this area showed no passes open into either Little Lagoon or Shelby Lakes, although some water possibly flows through the western inlet of Little Lagoon at the highest high tide. Between 1917 and 19 74, the gulf shore eroded by an average of -23. 8 km (-78 ft) between Fort Morgan and Alabama Point. This net erosion along the gulf shore oc- curred in the areas indicated on plate 1. Measurements of shoreline changes at 124 various locations identified on the Weeks Bay, Alabama, and the Foley, Alabama, 15-minute U. S. Geological Survey topographic maps are shown in table 13. Table 13. --Shoreline changes measured at identifiable points along gulf shore of Alabama Location @ne Time period Annual rate Mobile'Point +344 m (+1129 ft) 1917-1974 6. 04 m (19.8 ft) Gulf Highlands -31 m (-102 ft) 0.5 m (1. 8 ft) Gulf Shores indiscernible Romar Beach -47 m (-154 ft) 0. 8 m (2. 7 ft) Perdido Bay Perdido Bay is an estuary lying north of a bay-barrier complex that trends normal to the gulf shore at the Florida-Alabama state boundary. The Shores of Perdido Bay are well drained because elevations rise abruptly to 9 to 21 m (30 to 70 ft) on the west-central side of the bay and 1. 5 to 4. 6 m (5 to 15 ft) along the remaining; shore (Parker, 1968). Perdido Bay itself has shown little measurable change along the Alabama shoreline, according to presently available information. Areas of small amounts of erosion probably do exist within Perdido Bay but are too small to be discerned 125 by methods used in this study. Significant changes in the configuration of Perdido Bay have occurred in the area of Perdido Pass. Changes in the configuration of Perdido Pass are among the most extensive recorded in this study. Shorelines at various intervals between 1867 and 1974 are shown in figures 54 and 55. In 1867 the Perdido River channel (presently called Old River) flowed around the east end of Ono peninsula (now Ono Island) then west- ward to enter the gulf (fig. 54). By 1890-1892, this river channel had been partly abandoned and the major flow from Perdido Bay entered the gulf through a channel in Ono peninsula excavated by local residents between 1867 and 1892 (U.S. Army Corps of Engineers, 1973). By 1918, water exchange occurred through two inlets separated by an island (fig. 54). This configuration possibly was caused by the hurricane of September 8, 1917. Gradually the accretion resulting from the west- ward littoral drift closed these two inlets to form a single inlet by 1941 (fig. 55). Between 1941 and 1974, the persistent littoral drift had caused the pass to migrate westward until arrested by the construction of a seawall in the 1960's. Ryan (1969) mentions that the pass in its natural state was some 1. 8 m (6 ft) deep and presented great hazard to navigation. Safe navigation has been assured since the construction of several seawalls, which stabilize the inlet and protect a bridge over the inlet. PERDIDO PASS, 1867 TO 1890-92 .17"13' 87032' Land a 30077, Shoreli ONO IS L AND 7890-92 BP6 USE I B,AN 1919 ALAE@,@MA Shoreline indeterminate ecause.o.f lack of data" OLD RIVER .............. dX. .............................. 1890 8r33' 87032' PERDIDO PASS, 1890-92 TO 1918 gr 33, 8r32' Land ar 3 007 7' Shorelin .......... ...... ... . ...... 13 P0 U BAN 1919 Bpb U L Shoreline indeterminate because of lock,oi. 1918 OLD RIVER 1918 1918 XX, 1918 1918 0 2000 1 1 8r33' 8r3T FEET Figure-54. --Shoreline changes in Perdido Pass, 1867 to 1890-92, and 1890-92 to 1918. PERDIDO PASS, 1918 TO 1941 8r33' 87032' 30017, Nq Land area in 1918 1941 1941 Shoreline 1941 ONOISLAND BP6 USE 1934 1941 OWA :::@:::ALABAM 9 OLD RIVER iji: 1941 87033, 87032' PERDIDO PASS, 1941 TO 1974 .8-r 3 3.' 87032' .......... Land area in 1941 Shoreline 1960 @_j Shoreline 1974 @ONO IS BP6 USE 19 T L I N R ............... OLD RlV ............... BTi(]Cje ........... ...... ......... .............- ............ .................... ............ . .............. ................ 0 2000 B Jetty 87033' Br32' I FEET Figure 55. --Shoreline changes in Perdido Pass, 1918 to 1941, and 1941 to 1974. 128 The migration of the present inlet in the future is unlikely; however, past evidence suggests that a severe disturbance, such as a direct blow from a hurricane with its high tides and high current velocities, could again create one or more passes similar to those shown for 1918 (fig. 54). 129 LAND/WATER INTERFACE ANALYSIS Measurement of Alabama Shoreline Length Three different shoreline length mea surements are currently used for the State of Alabama. Appendix E of the National Shoreline Study prepared by the U.S. Army Corps of Engin eers lists the estuary shoreline length as 491. 2 km (305. 3 mi.), while the Alabama Department of Conservation states that the correct length is 577. 5 km (358. 9 mi.). N. 0. A. A. has published a value of 976. 7 km (607 mi.) for the length of tidal shoreline in Alabama. The Geological Survey of Alabama measured the shore- line and obtained a figure of 811.3 km (504.2 mi.), using an opisometer on large- scale maps. These measurements are based on traditional map analysis techniques and the difference between them manifests the difficulty encountered in such measure- ments, including the definition of the parameter being measured. Problems arise with subjective interpretation and the physical limitations of opisometry (map-wheel operation). The earth imagery acquired by the two NASA satellites, Landsat I and II, is a new source of information applicable to the problem in a format highly appropriate for automatic processing with digital computers. With data being collected- periodi- cally, repetitive analysis is feasible on at least an annual basis. This is particularly important in areas of dynamic geomorphology such as the upper reaches of Mobile Bay and the barrier islands. In addition, imagery may normally be obtained a short 130 time after the occurrence of hurricanes, which cause rapid and substantial changes to occur in coastal areas. Automatic processing of satellite imagery makes possible a raoid analysis of the large volume of data representing an area such as the coastal region of Alabama while simultaneously reducing the influence of human error on the analysis. Measure- ments based on the satellite data are not as subject to interpretation errors because they are based principally on objective analyses of quantitative data, as opposed to the subjective analysis of qualitative data representative of traditional techniques. The repetitive analysis provides the opportunity to readily identify any inconsistencies that might appear so that they can be resolved in a timely manner, while at the same time facilitating change detection. Because of the experimental nature of the automatic shoreline detection and measurement technique and the pilot aspect of this application, the resources dedicated to the Alabama shoreline measurement project were necessarily restricted. To. analyze the entire Alabama shoreline would require, given the available data, the pro- cessing of three computer-compatible tapes through the entire shoreline measurement system (which is outlined in appendix C). To improve confidence in the measurements, it was decided to analyze imagery from two dates covering the Alabama coastal area from the Mississippi state line east to longitude 87*421, near Foley. This excludes the 131 Perdido Bay area and requires only two computer- compatible tapes for each date. The shoreline segment east of Foley is being analyzed as a follow-on project. The inla'nd boundary of the measured area was determined by estimating the extent of tidal influence. Measurement of simple features in the Landsat images have agreed to within 8 percent of measurements of the same features on standard maps made with an opisometer. Data from December 28, 1972, and from December 5, 1973, were analyzed (figs. 56 and 57). Winter dates were chosen to minimize the effects of vegetation, which might obscure true shoreline or be floating in the marsh areas. Aerial photog- raphy acquired in February, 1973, (NASA Earth Resources Aircraft Project Flight No. 73-023) was compared with the computer land/water category classification. There was some difficulty in detecting thenarrow water courses in the marsh areas north and west of Mobile Bay, which demonstrates an effect of sensor resolution on the por- trayal of the scene. The detection of small streams at the coast was more complete in the 1972 data and may be the result of any of a number of factors including atmospheric conditions, vegetation state, and sensor performance. It is also likely that the streams were swollen at the time the 1972 data was collected. Discharge data for the Mobile River indicated a flow approximately one third greater in December of 1972 than in December, 1973. While the drainage areas for the streams in question are different 132 pr"amd by NASA/JSC EARTH RESOURCES LABORATORY NATIONAL SPACE TECHNOLOGY LAIMTORES BAY ST. LOUIS, MISSISSIPPI Figure 56. --Shoreline map showing limits of measured area irom Landsat imagery dated December 28, 1972. 133 p sp-r*d by NASA/JSC EARTH RESOURCES LABORATORY NATIONAL SPAC9 TECHNOLOGY LABORATORIES BAY ST. LOUIS, MISSISSIPPI 00@@ Figure 57. --Shoreline map showing limits of measured area from Landsat imagery dated December 5, 1973. 134 from the Mobile River basin, the Mobile River conditions were indicative of the entire area. Differences in the final shoreline measurement are due principally to the dif- ference in detection of the small streams and marsh land/water features. The tidal level was almost identical at the time of each image, so sea level change may be ig- nored. The edge of the screened pattern on the figures shows the inland boundary of the study area. The 1972 imagery yielded a land/water interface length in the coastal area of Alabama of 1,122.3 km (697.5 mi.), while the 1973 imagery was found to have a shore- line length of 87.8.5 km (546. 0 mi.). The analysis of Landsat data considers every de- tail of the shoreline that is detected at the resolution of the sensor, which is about 79. 2 m (260 ft) in the north-south direction and 58. 8 m (193 ft) in the east-west direction. While the same detail may in fact be present in the maps on which the previously published values are based, errors can easily be made in attempting to follow intricate shore- line features with an opisometer. This type of error would tend to decrease the meas- urement because of the straightening of the shoreline that would thus be effected. Deviation, between the two satellite-based measurements may be the result of differences in defining the areas upon which the analysis was performed, small errors in the factors for scaling and geometric correction of the imagery, or variations in the classification of land and water features in the scene. The fourth factor includes 135 actual geographic changes and misclassifications. This factor is apparent in' the marsh areas which are much more broken in the 1972 image and probably indicates a temporary or periodic change in actual surface conditions. The two shoreline length measurements derived from the Landsat data repre- sent two distinct conditions. The 1973 data are representative of normal river and stream conditions while the 1972 data represent the condition associated with high dis- charge conditions. A Landsat-based measurement of the Alabama shoreline from the Mississippi state line to 87421 longitude is 878. 5 km (546 mi.) under normal conditions. As stated above, NASA did not measure the entire shoreline of Alabama, since the coastal area east of 87'421, near Florida, was omitted. The Geological Survey of Alabama has derived an estimate of the total shoreline based on application of a ratio* obtained through conventional opisometer techniques. If the total length of Alabama's shoreline were measured using the NASA land/water interface technique, it would meas- ure approximately 1, 313 km (816 mi.). The ratio used is defined as opisometerpartial NASA-derived partia opisometer total x where x = total measurement of shoreline by NASA technique therefore 6 80. 6 km 1,000.4 km 811, 3 km X and x = 1,313.1 km or 816 mi. mean of NASA's 1972 and 1973 partial measurements .1 136 1 1 1 APPENDICES I I I I I I I I nI I I I I I 1 137 1 1 1 APPENDIX A I Landsat Imagery and Hydrologic Characteristics I I I I I - I I I 'I I I I I I I I I 138 Landsat- 1 1050- 15@60 September 11, 1972 1 meter 3 feet 2 1 0 0 -1 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 053-2 --------------- 0. 9 ebb 1855 --------------- 0. 9 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA-TOMBIGBEE Total discharge for September 1972 ----------- 15, 879. 7 m3/s (560, 787 cis) September 11, 1972, discharge --------------- 479. 6 m3/s (16,938 cfs) Mean discharge for September 1972 ----------- 529.4 m3/s (18,697 cfs) oil @LSA@T-1' 139 . . . . . . Landsat- 1 1086-15562 October 17, 1972 1 meter 3 feet LANDSAT-1 2 0- 0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 1212 ------------------- 1. 4 ebb 2357 ------------------- 1. 0 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA-TOMBIGBEE Total discharge for October 1972 ------------- 11, 401. 5 m3/s (402, 641 cf s) October 17, 1972, discharge ----------------- 292. 7 m3/s (10,336 cfs) Mean discharge for October 1972 ------------- 367. 7 m3/s (12,988 cfs) 140 N@ Landsat- 1 1158-15564 December 28, 1972 pop-, 1 meter 3 feet .2 LANDSAT-1 0- .0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0102 ------------------ 0. 5 ebb 1406 ------------------ 0.8 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA -TOMBIGBEE Total discharge for December 1972 --------------- 82,673.8 m3/s (2,919,602 cfs) December 28,1972, discharge -------------------- 2,814.8 m3/s (99,403 cfs) Mean discharge for December 1972 --------------- 2, 666. 6 m3/s (94, 170 cf s) 141 Landsat-1 1176-15562 January 15, 1973 1 meter 3 feet .2 0 0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0136 ------------------ 2. 6 ebb 1415 ------------------ 2.6 flood DISCHARGE CHARACTERISTICS FOR THE A LABAMA- TOMBIGBEE Total discharge for January 1973 ----------- 194, 678 m3 Is (6, 8 75, 0 10 cfs) January 15, 1973, discharge -------------- 5,678 m3/s (200,518 efs) Mean discharge for January 1973 ---------- 4,785 m3/s (168,985 cfs) 142 17 t-7, @r- @t Landsat-1 1194-15564 February 2, 1973 1 meter. 3 feet 2 1 LANDSAT-1 0 0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0429 ------------------ 2. 1 ebb 1730 ------------------ 1.9 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA- TOMBIGBEE Total discharge for February 1973 ---------- 157, 794.2 m3/s (5,572,457 cfs) February 2, 1973, discharge -------------- 3, 614. 6 m3/s (127, 651 cf s) Mean discharge for February 1973 --- @------3,434.4 m3/s (121,'285 cfs) 143 Landsat-1 1302-15565 May 21, 1973 'Iwo _4 1 meter 3 feet LANDSAT-1 2 0 1 0 2400 0400 0800 1200 1600 2000 2400 hrs MAYJMUM CURRENT Time Velocity (kts) 0720--l ------------------ 2. 0 flood 1936 -------------------- 2.0 ebb DISCHARGE CHARACTERISTICS FOR THE ALABAMA-TOM BIGBEE Total discharge for May 1973 ------------------- 123, 518 m3/s (4,361,534 cfs) May 21, 1975 discharge ------------------------ 1,903 m3/s (67,196 cfs) Mean discharge for May 1973 ------------------- 39,881. 6 m3/s (140,594 cfs) 144 ',X TE 4@ 3A,14:@1a Landsat- 1 1428-15550 September 24, 1973 J*- 1 meter 3 feet LANDSAT-1 -2 0. 0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0407 ------------------ 1. 1 flood 1443 ------------------ 0. 9 ebb DISCHARGE CHARACTERISTICS FOR THE A LABAMA- TOMBIGBEE Total discharge for September 1973 ----------- 17,227 m3/s (608,365 cfs) September 24, 1973, discharge --------------- 500 m3/s (17,687 cfs) Mean discharge for September 1973 ----------- 536.6 m3/s (18,953 cfs) 145 Landsat-1 1482-15541 November 17, 1973 1 meter- 3 feet -2 LAND .0 T -1 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0924 ------------------ 1. 5 ebb 2148 ------------------ 1. 0 flood DISCHARGE CHARACTERISTICS FOR THE A LABAMA- TOMBIGBEE Total discharge for November 1973 ------------ 26,012. 7 m3/s (918, 633 cfs) November 17, 1973, discharge ---------------- 642.3 m3/s (22,684 cfs) Mean discharge for November 1973 ------------ 8 10. 5 m3/s (28, 623 cf s) 146 Landsat- 1 1500-15535 December 5, 1973 -4k 1 meter. 3 feet 2 LANDSAT-1 1 0 0 2400 0400 0800 1200 1600 2000 2400 hrs MAXIMUM CURRENT Time Velocity (kts) 0146 ------------------ 0. 7 ebb 1430 ------------------ 0.8 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA-TOMBIGBEE Total discharge 'for December 1973 ------------ 73, 054 m3/s (2, 579, 885 cf s) December 5, 1973, discharge ---------------- 2, 220. 9 m3/s (78, 431 ef s) Mean discharge for December 1973 ----------- 2, 666. 6 m3/s (94, 171 cf s) 147 ,, A@rj Landsat-1 1806-15451 October 7, 1974 1 meter. 3 feet ANDSAT-1 2 0 1 0 2400 0400 0800 1200 1600 2000 2iOO hrs MA)UMUM CURRENT Time Velocity (kts) 0849 ------------------ 2.1 ebb 2111 ------------------ 2. 1 flood DISCHARGE CHARACTERISTICS FOR THE ALABAMA- TOMBIGBEE No data available 148 V, Kvl.@ ij WK, V, -1 1842-15441 Landsat November 12, 1974 t X, 1 meter. 3 feet 2 LANDSAT-1 0 -0 2400 0400 0800 1200 1600 2000 200 hrs MAXIMUM CURRENT Time Velocity (kts) 0241 ------------------- 1. 6 ebb 1553 ------------------- 1.7 flood DISCHARGE CHARACTERISTICS FOR THE A LABAMA- TOMBIGBEE No data available 1 149 1 1 I APPENDIX B I Source Material and Hydrologic Data I I t I I I I I I I I I 150 Table 1. --Selected photographic coverage available for Mobile Bay I)rpe of acquisition Data Date of platform type, format photography ,Landsat-I Prints-transparencies, B&W and 9-11-72 a few color composites 9-29-72 Scale: 1: 3, 369, 000 to 1:250, 000 10-17-72 12-28-72 1-15-73 2- 2-73 5-21-73 9-24-73 10-30-73 11-17-73 12- 5-73 6-21-74 9-19-74 10- 7-74 11-12-74 or transparencies Skylab 3 B&W, color, and color IR prints 8- 5-73 Scale: 1:2, 850, 000 to 1:250, 000 Skylab 4 B&W, color, and color IR prints 1-21-74 or transparencies Scale: 1: 2, 850, 000 to 1:250, 000 U-2 aircraft Color IR 9-24-72 Scale: 1:130,000 U-2 Color IR 2-22-73 Scale: 1:130,000 U-2 Color IR 10-17-.74 Scale: 1:130, 000 RB-57 F aircraft Color IR (post-hurricane Camille, 8-19-69 quite a few clouds) Scale: 1:130,000 Low-altitude aircraft B&W photos and photo mosaics 1938,1940, Scale: 1:20,000 and 1:64360 1949,1950, 1955,1960, 1966 151 Table 2. --Monthly discharge averages for the Alabama River (1931-1965) and Tombigbee River (1929-1960)* Monthly M3/s ft3 /s October 566.1 19,989.7 November 835.1 29,489.2 December 1,600.0 56,496.0 January 2,646.6 93,453.8 February 3,349.0 118,256.4 March 3,824.5 135,044.7 April 3,563.9 125,842..7 May 1,736.6 61,321.7 June 914.2 32,281.9 July 914.8 32,303.3 August 744.4 26,285.6 September 579.5 20,462.7 NOTE: In order to obtain the full discharge into Mobile Bay, the figures for the combined rivers were multiplied by 1. 07. Source: U. S. Geological Survey, Surface Water Records, 1929-1960. 152 Table 3. --Suspended sediment (12-year monthly average), Tombigbee and Alabama River systems from 1952 to 1963 (Compiled from unpublished data, U.S. Corps of Engineers, Mobile District) Tombigbee River Alabama River Combined Month M. tons Sh. tons M. tons Sh. tons M. tons Sh. tons January 304,454 (335,661) 218,502 (240,899) 522,956 076,560) February 470,903 (519,171) 349,988 (385,863) 820,892 (9 05,034) March 506,559 (558,482) 429,001 (472,974) 935,560 (1,031,456) April 343,.529 (378,742) 397,015 (437,710) 7401) 545 (816,452) May 164,647 (181,524) 187,768 (207,015) 352,416 (388,539) June 43,766 48,253) 102 116 (112,583) 145,882 (160,836) July 65,272 71,963) 79,899 88,089) 145,171 (160,05.2) August 11,163 12,308) 38,657 42,620) 49,821 ( 54,928) Septe mber 12,511 13,794) 44,640 (49,216) 57,151 ( 63,010) ,D ctober 16,934 18,670) 40,408 (44,550) 57,342 ( 63,220) November 59,436 65, 529) 47,137 (51,969) 106,.574 (11T,498) Oecember 173,324 (191,090) 169 315 (186,670) 342,636 (377,760) Annual 2,172,503 (2,395,187) 2,104,446 (2,320,158) 4,276,949(4,715,345) totals 1 . Based on daily suspended sediment data. 2. Station near Leroy, Ala. 3. Station at Claiborne, Ala. (After Ryan 1969) 153 Table 4. -'Yearly discharge averages into Mobile Bay by the Alabama- ITombigbee Rivers (1931-1974) Year M3/s ft3/s 1931 1,052.7 37,171.8 1932 1,837.3 64,874.1 1933 2,630.9 92,897.4 1934 1,066.9 37,674.7 1935 1,767.5 62,413.1 1936 1,985.1 70,095.7 1937 1,922.7 67,891.5 1938 1,850.6 65,344.9 1939 1,835.4 64,809.9 1940 1,636.3 57,780.0 1941 1,066.3 37,653.3 1942 1,342.7 47,411.7 1943 1,623.6 57,330.6 1944 2,012.4 71,058.7 1945 1,606.9 56,742.1 1946 2,580.3 91,110.5 1947 2,158.8 76,226.8 1948 1,964.2 69,357.4 154 Table 4. --Yearly discharge averages into Mobile Bay by the Al abama- Tombigbee Rivers (193 1- 1974)-- Continued Year M3/s ft3/s. 1949 3,050.2 107,706.2 1950 1,684.5 59,481.3 1951 1,744.2 61,589.2 1952 1,484.8 52,430.0 1953 1,716.3 60,604.8 1954 1,097.5 38,755.4 1955 1,257.8 44,415.7 1956 1,326.9 46,855.3 1957 1,517.8 53,596.3 1958 2,116.9 76,515.7 1959 1,345.4 47,508.0 1960 1,630.9 57,587.4 1961 2,245.4 79,287.0 1962 2,517.5 88,895.6 1963 1,360.0 48,021.6 1964 2,323.9 82,058.3 1965 1,736.6 61,321.7 1966 1,514.5 53,478.6 155 Table 4. --Yearly discharge averages into Mobile Bay by the Alabama- Tombigbee Rivers-- Continued Year M3/s ft3/s 1967 1,259.0 44,458.5 1968 1,969.3 69,539.3 1969 1,500.2 52,975.7 1970 1,456,0 51,413.5 1971 1,994.2 70,416.7 1972 1,760.5 62,167.0 1973 2,726.6 96,278.6 1974 2,278.7 80,464.0 156 Table 5.-- Selected charts and maps available for the Alabama coastal area U.S.G.S. 7k' Quadrangles Publication Date Mobile 1953-1967 Hollingers Island 1953-1967 Belle fontaine 1956 Little Dauphin Island 1958 Heron Bay 1958 Isle aux Herbes 1958 Kreole 1958 Grand Bay S. W. 1958 Grand Bay 1967 Coden 1956 Petit Bois Island 1958 Fort Morgan N. W. -1958 Fort Morgan 1958 Bridgehead 1953-1967 Daphne 1953-1967 'Point Clear 1956 Lillian 1970 W. Pensacola 1970 Perdido Bay 1970 U.S.G.S. 15' Quadrangles Weeks Bay 1941 Grand Bay- 1958 Foley 1941 157 Table 5. --Selected charts and maps available for the Alabama coastal area-- Continued U. S. G. S. 1:250, 000 National Topographic Maps Pensacola, Fla.; Ala. 1957-1970 Mobile, Ala. ; Miss. ; La. 1953-1970 U. S. G. S. 1:500, 000 Base map of Alabama 1966 National Ocean Survey Nautical Charts Chart No. Scale Date 91 1:80,000 1860 187 1:80,000 1897 187 1:80,000 1916 188 1:80,000 1909 188 1:80,000 1894 189 1:80,000 1894 189 1:80,000 1909 189 1:809000 1918 874 1:40,000 1947 1266 1:80,000 1921 1266 1:80,000 1929 J266 1:80.9000 1943 1266 1:80,000 1973 1267 1:80,000 1920 1267 1:80POOO 1921 1267 1:80,000 1933 1267 1:80,1000 1944 11374 (Formerly 874-SC) 1:401000 1974 11378 (Formerly 874-SC) 1:40,000 1974 158 Continued Table 5.-- Selected charts and maps available for the Alabama coastal area-- Miscellaneous U.S.C. & G.S. Topographic Sheets 1:40,000-Scale 3702 1917 3711 1917 3712 1918 3713 1918 3714 1918 3716 1918-1919 1:10,000-Scale 5497 1934 5498 1934 5528 1934 5529 1934 5530 1934 5531 1934 5532 Supp. 1934 5533 1934 5534 1934 5535 1934 5536 1934 5537 1934 Miscellaneous Maps Carte de L'Isle Dauphine, ses Environs, par le S' DuSault, 1917 Historic Dauphin Island, by E. Wilson, 1971 .1 159 1 1 I APPENDIX C I Automatic Processing of Satellite Data for Shoreline Measurement I I I I I - I I I I I I I I 160 APPENDIX C AUTOMATIC PROCESSING OF SATELLITE DATA FOR SHORELINE MEASUREMENT The NASA satellite Landsat (formerly the Earth Resources Technology Satellite) provides imagery of the earth's surface in a format suited for auto- matic processing. Analysis of the light intensity in different regions of the opti- cal spectrum allows one to discriminate land from water. Further processing makes possible the measurement of the land/water interface and generation of a thematic presentation showing the land and water and the shoreline that was measured. Data Acquisition System The sensor used to acquire data on Landsat is a multispectral scanner. This is a device which, at any given instant in time, views a very small area approxi- mately 79 m (259 ft) on a side. This area is called the instantaneous field of view (IFOV) of the sensor. The IFOV is scanned along a line perpendicular to the motion of the satellite, which itself travels along a line oriented approximately north-south. The extent of the scan is about 5 degrees from nadir in either direction across the satellite ground track, and results in a coverage of 18 5 km (100 nautical mi.) in an east-west direction. By the time that the system completes one scan and is ready to scan again, the satellite has moved down its track and the next scan line is offset from 161 the previous line. The data taken at this time is adjacent to the previous line of data, and juxtaposition of successive scan lines generated in this way produces the two-dimensional image. As the term multispectral implies, the scanner is viewing the earth beneath in different regions of the electromagnetic spectrum. The radiation received by the scanner is broken down into green light (0. 5-0. 6 micrometers (Rm) ), red light (0. 6-0. 7 um), and two bands of infrared light (0. 7-0.8 and 0. 8-1. 1)1m). The intensity of the radiation in each of these four spectral bands is simultaneously measured and recorded for each picture element, which is defined as an individual sample point on the scan line. The picture element represents a spot on the earth with dimensions of about 79 by 58 m (259 by 190 ft). Multispectral scanner data is well suited for earth surface studies because the data from each of the four spectral bands are readily available in a computer- compatible form for automatic processing. Spectral signature analysis can be per- formed directly on flis data to generate images, with each picture element classified into predetermined categories. For shoreline analysis, the computer is programmed to recognize *the spectral signature of water and to classify those picture elements which it recognizes to be water, and to leave all other picture elements unclassified, which set then corresponds to land. There are problems involved with the use of this type of data for analysis of surface features, notably the geometric distortions inherent with scanner data. Cor- rections can be made for rotation of the earth beneath the satellite, the angular 162 displacement of the scan direction from the exact perpendicular to the satellite ground track, and variation of the width of the picture elements along the scan line. First-order corrections for the earth rotation and for the varying picture element size were made in the shoreline length analysis described in this docu- ment, while the second problem was deemed to have a negligible effect. Better correction techniques now eki'st, and are being implemented, but were not avail- able at the time this work was performed. Procedure for Shoreline Measurement There are nine basic steps outlined in figure Cl@that are required to derive a display showing land, water, and shoreline and the length of the shoreline from the Landsat multispectral scanner data. The data are originally provided in the form of a film image of the earth scene as recorded for each of the four spectral channels. Initial examination of the film images determines the suitability of the frame of data for analysis - whether the area to be studied is completely included in the frame, whether clouds will interfere with the analysis, and so on. If the frame is suitable for analysis, the digital magnetic tapes containing the values of light intensity for each spectral band for each picture element are obtained. All subsequent work is based on these digital data. The next step in the procedure is to determine the spectral signature of water so that the computer can be instructed to recognize water and classify it. 163 Film SELECT NEW STEP I FLAME SUIT" us TRAIN LANDIWATER STEP 2 CLASSIFIER CLASSIFY EN, 1RE STEP 3 DATA SET COMPARE REVISE CLALSSIFICtITZON STEP 5 CLASSIFIER WrIH . PHvrOC:RAPHY STEP 4 140 A Mar YES ISOLATE AREA FOR ANALYSIS STEP 6 DETERMINE SCALE OF STEP 7 124ACERY AND SKEW CORRECTION DETECr AND MEASURE STEP 8 SHORELINE ME PAT 9 DISPLAY OF STEP 9 /WATER/SHORELINE Figure C1. --Flow of processing to perform shoreline length analysis on YES Landsat MSS data. 164 Areas known to be land and areas known to be water are located in the data. Values of radiation intensity in the green and second infrared spectral bands are then ex- tracted for each of the picture elements in these land and water areas. These areas are known as training samples because data from them are used to "train" the com- puter to recognize the two categories. A graph with axes representing the green-band intensity and the infrared-band intensity is developed, with data points corresponding to land features differentiated from.those which correspond to water f eatures (fig. C2). A line is then drawn through the data that best separates the two sets of points. This line defines the land/water discriminator that will then classify each picture element on the basis of intensity of green and infrared light. The second infrared band alone provides a very good definition of land and water because water strongly absorbs radiation in that spectral region, where very strong reflectance is typical of land features. The intensity of green light reflected from the area being classified serves to adjust the decision point in the infrared for varying turbidity levels of the water, which can cause problems in areas of muddy river discharges and marshes. The third step in the procedure is to examine each data point in the frame and compare the light-intensity measurements in the green and infrared bands to the land/water decision curve. The computer tests these data and determines whether they match more closely the spectral signature of land or of water, and then classi- fies accordingly that picture element. From this classification process, a new @165 30 - 0 x 0 x 25 - 0 0 x x x x x X LAND 0 0 0 0 0 x x 0 WATER 0 0 x x x 20 -o o x x x x x x 0 0 X X X X ,Z I x X X tt 0 0 x x x '@?,O' 15 o tTl 0 0 5 0 0 5 10 15 20 INFRARED INTENSITY 0.8-1.1/UM f 0 x oxx x Figure C2. --Land/water discrimination using Landsat MSS data. 166 magnetic tape is generated that portrays each picture element with a code cor- "Tesp g to either land or water. After the image is classified, it is then closely examined and compared to aerial photography of the area acquired thin,.a-re sonable time period of the satellite data acquisition. The accepta- -@Wi a ble time period is determined by the rate of change of the geography and the problems expected in the classification. Marsh areas generally are the most diffi cult to classify and also the most dynamic, so when marsh areas are to be classified there should be aerial photography for comparison not more than a year or two before or after the date of the satellite image. If the comparison shows that there are serious. discrepancies between the classification and the visual interpretation of the photography, the land/water discriminator must be modified. The most common cause for such discrepancies is that the training samples are not representative of all regions found in the data set.: After modi- fying the discriminator, the classification process is repeated and the results are compared to the photography. Th ese steps are repeated until a satisfactory land/ water thematic has been generated. Because a Landsat image will typically contain not only the immediate coastal .area in which one wants to measure the land/water interface, but also the inland region containing small ponds;, lakes, creeks, and rivers, the coastal area must be isolated. The image is displayed and the limits of the area to be analy zed are 167, determined. The code for each picture element outside the area of consideration is then switched from either land or water to a third code that will be recognizied by subsequent computer analysis and ignored. The image is then ready for d6- tection and measurement of the shoreline. The satellite data must be scaled accurately for the shoreline measurement to be meaningful. Nominal values are given for the picture element dimensions, but@,Ithese may vary significantly. Good results have been obtained in scaling the data by locating points identifiable in the satellite imagery on accurate maps. The distances between these points are measured on the maps, and the number of picture elements separating the points in the satellite imagery along the scan direction and perpendicular to it are determined. In addition to the simple scaling, a correction must be made for the rotation of the earth beneath the satellite, referred to as skew' correction. Both the scaling and skew correction factor are determined using dis- tances measured on the map and in terms of .picture element offsets in the image. A least squares error technique is used to compute the picture element "width" and "height" and the skew correction factor, which is consistently equivalent to approxi- mately one element offset every eleven scan lines. With these factors determined, the shoreline may be detected and measured. A shoreline element is defined as the edge of an element of water which is adjacent 168 to an element of land. A two element wide and two element high "window" is scanned over the classified image, and each element of shoreline is noted. There are four basic types of shoreline elements: horizontal (twowater elements in one scan line, two land inthe other); vertical (the first element of each scan line within the window is land and the second is water); diagonal (fig. C3); and corner (fig. C4). Each of these types has a different length, so the number of each type of shoreline element is accumulated for the entire image. After scan- ning the entire image, the number of each type of shoreline element is multiplied by the length for the respective type, and these products are then summed to.give the total interface length. The horizontal and vertical elements contribute one picture element width and height respectively. The diagonal contribution is the square root of the sum of the squares of the width and height, corresponding exactly to the diagonal measure of the picture element. Because sharp corners are not typical of natural scenes, the contribution of such apparent features is that of a rounded corner - the length being one half the'width plus one half the height of the picture element, plus one quarter of the average of the perimeters of the ellipses that can be inscribed and circumscribed on the picture element. The computer program that detects and measures shoreline also generates a new image of the scene. This image has been modified from that generated by the 169 ....... .......... ........... . ............ ........... ....................... Figure C3. --One configuration of land (1) and water (2) whicli indicates a diagonal interface feature. Shaded area is examinatLon window. .......... .... .......... ..I........ ........... .......... ... ............ .......... 2 ............ .......... ...................... Figure C4. --One configuration of land (1) and water (2) which indicates a corner interface, feature which must be rounded in the length computation. 170 land/water classifier to show as a fourth class every element of water found to be adjacent to an element of land. The shoreline image, as this new image is called, shows land, water, shoreline, and areas excluded from analysis. 171 REFERENCES Austin, G. B. , 19 54, On the circulation and tidal flushing of Mobile Bay, pt. 1: Texas Agr. and Mech. Coll. Dept. Oceanography unpub. paper, proj. 24, 28 p. Avrett, J. R., 1966, A compilation of surface water quality data in Alabama: Alabama Geol. Survey Circ. 36, 57 p. Bird, E. C. F. , 1969, Coasts, v. 4 of An introduction to systematic geomor- phology: Cambridge, Massachusetts, M. I. T. Press, 246 p. Boone, P. A. 9 1972, Descriptive geology of southwest Alabama and the adjacent continental shelf: Alabama Geol. 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