Beach erosion in South Carolina

[From the U.S. Government Printing Office, www.gpo.gov]

15404

COASTAL ZONE
INFORMATION CENTER

BEACH EROSION
IN SOUTH CAROLINA

CZIC COLLECTION

Miles 0. Hayes, Thomas F. Moslow
and
Dennis K. Hubbard

GB
459.4
S6
H41-8
.1979

South Carolinea Coastal Council

[email protected] 4 (JI-i

COASTAL ZONE
INFORMATION CENTER
BEACH EROSION IN SOUTH CAROLIX

Miles 0. Hayes Thomas F. Moslow
and 2
Denni K. Hubbard

C Library
property 01 CS
[email protected] COLLECTION

---w Preparation of this document was financed in part through
grant assistance from the U. S. Department of Commerce,
National Oceanic and Atmospheric Administration, Office
of Coastal Zone Management, Grant No. 04-7-158-44141,
pursuant to Public Law 92-583.
0
C)

U DEPARTMENT OF -COMMERCE NOAA
4- COASTAL SERVICES CENTER
V VENUE
IT 2234 SOUTH HOBSON A 05-2413
0 '. i Coastal Research Division CHARLESTON SC 294
Department of Geology
University of South Carolina
Columbia, S. C. 29208

2
West Indies Laboratory
Farleigh Dickinson University
Christiansted, St. Croix
Maw-
U.S. Virgin Islands, 00820

[email protected]

TABLE OF CONTENTS PAGE

INTRODUCTION ................................................................... 2

Climate ................................................................... 2

Waves ..................................................................... 3

Longshore Transport ....................................................... 3

Tides ..................................................................... 5

GENERAL COASTAL MORPHOLOGY ..................................................... 8

Arcuate Strand ............................................................ 8

Cuspate Dei-ta ............................................................ 10

Barrier Islands ......................................................... 12

Beach-ridge barriers ............................................... 12
Transgressive barriers ............................................... 12

Nearshore Bathymetry ..................................................... 13

Characteristics of South Carolina Beach Sand ............................. 13

COASTAL PROCESSES AND BEACH EROSION ........................................... 14

Beach Erosion - An Overview .............................................. 14

Causes of Beach Erosion .................................................. 19

Wave attack ......................................................... 19

Storm surge .......................................................... 23

Hurr4canes .......................................................... 23

Sea level rise ...................................................... 27

EROSION-DEPOSITION TRENDS ..................................................... 29

SHORT TERM CIIANGES,,**.****,,,.***,**...,***...* .... ** ... *- , -- 36

What is' a beach profile? ................................................. 36

Data Presentation ........................................................ 36

Grand Strand ........................................................ 39
Debidue and North Islands ........................................... 39
Cape Romain ........................................................ 43
Capers-Bull Islands ................................................ 43
Isle of Palms....' ***"**'* ... ***'*'""''***'******'*"**'********', 43
Sullivans Island ................................................... 45
Folly Beach ......................................................... 45
Kiawah Island ...................................................... 47
Edisto Beach ........................................................ 51
Hunting Island ....................................................... 52
Hilton Head Island ................................................... 52
LONG-'TER1,1 CHANGES ........................................................... 55
Study Procedure .......................................................... 55

Data Presentation ........................................................ 56

SUMMARY ..................................................................... 91

ACKNOWLEDGEMENTS ............................................................ 93

GLOSSARY ................................................................... 94

REFERENCES .................................................................. 97

SYNOPSIS

A characterization of beach erosion trends along South Carolina's shoreline

has been based on beach profiles, beach processes and erosional-depositional

hiEtory. Four coastal types have been identified: 1) arcuate strand, 2) cus-

pate delta, 3) beach-ridge barrier, and 4) transgressive barrier. The arcuate

strand extends from the North Carolina border to Winyah Bay and is characterized

by a stable, continuous beach, broken by few tidal inlets. This area has eroded

to the extent that the modern beach presently rests against beach ridges dated

at 100,000 years old. The-cuspate delta, lying between Winyah Bay and Bulls

Bay, contains a cuspate foreland, Cape Romain, which is characterized by an

eroding headland, elongating spits on the flanks of the headland, and an over-

all erosional nature. Beach-ridge barrier islands, which comprise the bulk of

the central and southern portions of the coast, are composed of vegetated beach

ridges. Transgressive barrier island areas (Morris Island, Edingsv ille Beach

and Bay Point), which are characterized by straight beaches, are rapidly re-

treating landward through a washover mechanism. Charts dating back to 1779

show evidence of beach ridges in some areas which have since eroded away.

These studies have lead to the following conclusions:

1) Erosion rates along the South Carolina coast are typically 10 inches

(30 cm) to 3 feet ( 1 m ) per year.

2) The area north of Winyah Bay is generally stable due to the nature of the

underlying sediments.

3) The rest of the coast exhibits varying degrees of instability depending on

the character of the backshore area and the size and occurrence of tidal in-

lets. Areas backed by well-developed beach ridges characteristically have

lower short-term erosion rates than those where such features are absent.

4) Beach-ridge barriers longer than approximately 6 miles ( 9km) are com-

posed of unstable, bulbous updrift ends, stable or accretional central

portions, and progradational downdrift ends, which give the islands a drumstick-

like shape. Beach-ridge barriers shorter than approximately 6 miles ( 9km)

show large and sporadic changes along their entire le ngth in response to changes

in neighboring tidal inlets.

Little R.
J LO

@[email protected]

North

.rPrice

Dewees.

- - - - - - - - - - -

ston

disto,

St. Helena Sd.

Fripp

Pt. Royal Sd-

0 3o krn F4

Figure 1. Location map of the South Carolina coastal zone. Those inlets
shown in the insets,are: A) Little River, B) Murrells, C) Dewees, D) Capers,
E) Price, F) Stono, and G) Fripp. (from Hubbard and Barwis, 1977).

INTRODUCTION

Beaches and barrier islands of South Carolina comprise one of the state's

most valuable natural resources (Fig. 1). The beaches are the greatest single

attraction for the state's billion dollar tourism industry., In 1975 alone,

more than six million vacationers stayed at lodging places and campgrounds

in the coastal area, accounting for over 400 million dollars of the state's

35
tourism revenue Therefore, it is of considerable economic interest to

preserve and enhance the quality of the state's beaches. Unfortunately, many

of the beach areas are threatened by severe erosion problems, some of which

have been fostered by unwise construction and development techniques.

The primary goal of this report is to examine both the beach erosion

trends and the dynamic processes responsible for them along the South Carolina

coastline. Stable beach areas and areas of critical erosion are identified

on the basis of studies of historical charts and maps, vertical aerial photo-

graphs and systematic measurements of shoreline changes carried out over a

three-year period at over 70 field stations. Limits for set-back lines,

which define areas suitable or unsuitable for development, are defined in a

general way from the erosion-deposition graphs presented. The data are pre-

sented in a format that should be of use to state and federal agencies, de-

velopers, homeowners, and groups interested in the environment of the state.

However, some caution should be exercised in using the graphs and tables as

the solle means for making development decisions. In many locations, site-

specific studies should be carried out by experts in coastal processes and

engineering before final decisions are made regarding treatment of the ero-

sion problem.

Climate

South Carolina's climate is mild, with an average temperature for the
coastal region of 650F, ranging from 50 0F in December to 810F in Ju ly.

The coastal plain, which makes up 40% of the state, receives an average of

26
46.5 inches of precipitation annually An average of 1.4 hurricanes and

tropical storms affect South Carolina's coast annually, although none have
occurred for many years 4

On an annual scale, no predominant direction of wind approach is apparent

along South Carolina's coast (Fig. 2). However, seasonal trends can be seen.

During the spring and summer, winds from the south and southwest prevail;
whereas, in the fall and winter, most winds come from northerly directions. 40

Shipboard wind and wave observations were used to derive wind and wave fre-

quency distributions for the Charleston area (Fig. 3). Wave energy values

(fluxes) show the same seasonal trends as the wind.

Waves

Wind-produced waves are the most dominant natural force affecting erosion-

al-depositional trends along the coastal zone. The longer and stronger the

wind blows (duration) and the greater the distance over which it blows (fetch),

the larger and more powerful the waves will be. During storms, wave energy

can carry beach sands seaward and damage or carry away man-made structures.

During calm periods, waves move offshore sand onto the beaches, building them

UP.

Longshore Transport

The most important currents affecting shoreline changes are longshore

currents. These are produced by waves that strike the coast at an oblique

angle and run parallel to the shoreline. Longshore currents vary in velocity

and direction with wave angle and wave energy. The combined forces of long-

shore currents and wave action result in the movement of large volumes of

sand parallel to the coast. This is referred to as longshore transport.

WIND ROSES

SP04G SUMMER

% 0
2MO AN L

FALL WINTER

Figure 2. -Seasonal and annual wind roses for the South Carolina
coast. (from Brown, 1977).

ENERGY FLUXES

SPR" SUMMER

PLS
0
@21 [email protected] KM
(X)06 G MISW).a A4
4"03 ANNUAL

F"L WINTER
---"7 5U"

Figure 3. Seasonal and annual wave energy values for alongshore and
onshore winds in the Charleston area. The length of any bar is
a relative measure of the wave energy coming from that direction
(from Brown, 1977).

Along the South Carolina coast, the dominant direction of longshore transport

is to the south. The directions and rates of longshore transport for the cen-

tral South Carolina coast are given in Figure 4.

When sediment is scarce, longshore transport will carry sand away from

the beaches, causing erosion. However, this sand may eventually be deposited

on beaches downdrift by natural processes or man-made structures, or it may

also be carried seaward and deposited offshore.

Tides

The fluctuation of daily tides along the South Carolina coast can be a

big factor in shoreline erosion. This is especially true when storms pile

up tide levels, resulting in the flooding of low areas along the coast. Tide-

produced currents are especially strong at harbor entrances or at inlets to

lagoons or bays. Flood tides can sweep sediments Irom the longshore transport

system into a bay or tidal marsh area. Ebb-tidal currents, which are more

dominant along the South Carolina coast, can deposit sediments at the mouths

of inlets or add material to the longshore transport of sediments. During

hurricanes and storms, coastal areas which are normally safeguarded from wave

30
attack may undergo severe wave erosion if the storm comes at high tide.

South Carolina has a mixed wave and tidal energy coast with tidal in-

fluence increasing to the south. Mean tidal range shows a gradual increase

from North Carolina to Georgia (Fig. 5). Mean tidal range at the North Caro-

lina-South Carolina border is 5 ft. (150 cm) compared to 6.5 ft. (200 cm)

along the southern coast. This change is largely controlled by nearshore

bathymetry and the general shape of the coastline.

The increase in tidal range from north to south and the resulting in-

crease in tidal prism has several effects on the South Carolina coastline:

1) Tidal inlets become more frequent and are larger to accommodate greater

tidal flow; 2) Salt marshes are more extensive; and 3) The ebb-tidal deltas

LONGSHORE TRANSPORT RATES DEBIDUE
ISLAND
FOR CENTRAL SOUTH CAROLINA 150,000
.1/y,

BULL ISLAND

139,000 Y,
131,000,M,/y,
"CAPERS ISLAND ATLANTIC OCEAN
289,000 /y,

/TRANSPORT DIRECTION

Figure 4. Location map and longshore transport rates for the
central South Carolina coast. (from Kana and Knoth, 1977).

SPRING TIDAL RANGE VARIATION

GA.

0
KM

280

240 ?40

200 200

160
-160

120 120 0A.

Figure 5. Spring tidal range variation along the shoreline of
South Carolina. Note increase in southerly direction. (from
Brown, 1977).

become much larger off the inlets and estuaries in the southern portions of the

2
state GENERAL COASTAL MORPHOLOGY

The morphology of the South Carolina coast is a transition between that

of North Carolina and Georgia., North Carolina's coast is predominantly made

up of long, thin barrier islands broken up by a few tidal inlets. The morpho-

logy of the North Carolina coast is controlled mainly by wind-generated waves

and currents. Georgia's coast is comprised of short, stubby barriers separated
by many large tidal inlets, typical of tidal-current-controlled coasts 11.

The mor phology of the South Carolina coast is dominated by a mixture of the

wind-generated and tidal-generated forces.

On the basis of geomorphology, the South Carolina coastlis classified in-

to the arcuate strand, cuspate delta and barrier island zones. The barrier

island zone is further divided into islands that have beach-ridges (beach-ridge

barriers) and those that have no beach ridges (transgressive barriers) (Fig. 6).

Each of these four divisions has its own characteristic sediment type, bathymet-

ry and erosional-depositional history.

Arcuate Strand

The arcuate strand (Fig. 6) forms a gentle crescent between the North

Carolina border and Winyah Bay, a distance of approximately 60 miles (100 km).

Few tidal inlets breach the coast in the northern section, but the number of

inlets increases south toward Winyah Bay. Inlet size also increases southward.

This portion of the coast is normally backed by a well-developed dune system.

Salt marshes are poorly developed or totally absent in the north and central

portions ofthe strand, but become more prominent in the southern section. This

section of coastline appears generally stable with the exception of the areas

in the vicinity of tidal inlets.

34-

VARIATIONS IN
SOUTH CAROLINA
COASTAL MORPHOLOGY MYRTLE REACH

WINYAH BAY

DELTA
SANTEE
3r-
CAPE ROMAIN

8"LL BAY

CHARLESTONO
MORRIS ISLAM
-- ---- ARCUATE STRAND
EDINGSVILLE BEACH CUSPATE DELTA
BEAUFORT =BEACH RIDGE BARRIER
dBAY PCXNT =TRANSGRESSIVE BARRIER

HILTON HEAD 0 so
KM 32-

iigure 6. Map of the South Carolina coast sho-,Jinc, the four major
morphologic zones. (from Brown, 1977).

The shoreline owes its stability to the barrier sands of the Myrtle Beach

Formation which formed before the Wisconsin glacial period, approximately 100,
000 years ago 21 . The present shoreline configuration generally parallels the

orientation of these resistant relict beach ridges.

Cuspate Delta

The Santee River Delta, which extends 18.5 miles (30 km) along the South

Carolina coast, is the largest deltaic complex on the east coast of the U. S.
It is classIified as a wave-dominated cuspate delta 33. The shoreline components

of the delta include: 1) a cuspate foreland, Cape Romain; 2) an eroding beach-

barrier complex, Raccoon Key; and 3) distributary mouth sand bars and mud flats.

The lower delta plain is presently covered by salt marsh. The sand which com-

prises the delta was originally supplied by the Santee River. Subsequent ero-

sion by predominantly northeast storm waves has given the Cape its character

istic shape (Fig. 7). Erosion of the cape headland has caused its northern

flank to change orientation dramatically during the past century, shifting

from N-S in 1886 to its present NNE-SSW orientation. Since 1886, the northern

arm of the cape has elongated approximately 1.1 mile (1.8 kin), while the west-

34
ward arm grew a length of 2.3 miles (3.7 km) . The washover terraces and

truncated beach ridges along the shoreline of the delta attest to its rapid re-

treat. Erosion of the Santee delta complex has been related to the decreased
sediment supply after damming of the Santee River in 1942 1. Prior to the

1930's, the delta was in a stable or constructional phase. After that, the

delta entered a destructive phase which presently continues. Sequential ver-

tical aerial photographs reveal that, in some cases, over 615 ft. (215 m) of

37
erosion has occurred since 1941 along Cape Romain . Along Raccoon Key, to

the south, erosion of up to 900 ft. (275 m) was noted at some localities. The

proposed rediversion of the fresh water discharge back into the Santee River

is expected to have little beneficial effect as most of the sand-sized material

k '5R""-
"@p
AP
[email protected][email protected]

Figure 7. Oblique aerial view of Cape Romain (photo taken October
1974). (Brown, 1977)

[email protected]

Figure 8. Oblique
southerly aerial
view of a series
-ridge
of beach
S barrier islands.
- - - - - - - - - -
Capers Island is
in the foreground.
Photo taken in
February 1975
(from Brown, 1977).
Sm,

. . . . . . . . . . .

V
[email protected]

will still be retained by upstream dams.

Barrier Islands

Between Bull Bay and the Georgia border, a distance of approximately 100
miles (160 Ian), a series of barrier islands front the coast. They'average

about 4.5 miles (7 km) in length and are separated from the shoreline by a

zone of salt marsh which generally increases in width toward the south. Numer-

ous tidal inlets separate the islands. These islands are of two types, beach-

ridge barriers and transgressive (erosional) barriers.

Beach-ridge barriers comprise the majority of the central and southern

portions of the South Carolina coast. These areas are characterized by exten-

sive beach ridges, formed as the shoreline prograded. These ridges act as

partial buffers to erosion; barriers with beach ridges generally show less

variability than do those without ridges (Fig. 8). The morphology of these

barriers is greatly affected by the adjacent tidal inlets. Wave refraction

and storm protection afforded by the ebb-tidal delta can cause accretion on

12
the adjacent beach, resulting in a bulbous updrift end of the island

The larger barriers often exhibit a straight to crescentic central portion

and a downdrift end which elongates and progrades through the formation of re-

curved spits. In areas where the barriers are shorter (Capers Island, Dewees

Island) or the inlets much larger (Hilton Head Is.), this pattern becomes more

complex. Migration of the inlets can further extend their influence.

Transgressive barrier shorelines are of lower relief and exhibit typi-

cally higher rates of erosion, T hey are characteristically straight and are

a thin veneer of sand which retreats landward as a succession of washovers.

Sequential charts and ae rial photographs show that transgressive barriers

can be the erosional end-product of beach-ridge barriers. Historic coastal

charts of Morris Island and Edingsville Beach show that beach ridges existed

in 1779. Lacking the local relief and storm protection provided by dunes and

beach ridges, transgressive barriers are presently changing at an extremely

rapid rate. Erosion rates of up to 50 ft. (15 m)/yr. have been documented

37
at Morris Island . Evidence of such rapid rates of erosion can be observed

in the outcropping of marsh peat along some of the transgressive barrier

beaches.

Nearshore Bathymetry

There is a significant change in bathymetry along South Carolina's coast.

North of Winyah Bay, typical profiles are concave and very steep.in the near-

shore. South of Winyah Bay, the influx of fluvial sediments and the storage

of sand in ebb-tidal delta complexes causes a decrease in nearshore slope, al-

though the overall slope to a depth of 50 ft. (15 m) is very uniform along the

entire coast (.5 ft./mi.). The area off Cape Romain has the most irregular

bathymetry due to the presence of cape-associated shoals. Bathymetry in the

barrier island portion of the coast is governed by proximity to tidal inlets.

No appreciable difference is apparent in the bathymetry between beach-ridge

and transgressive b arriers.

Characteristics of South Carolina Beach Sand

When sand grain size and sorting parameters are plotted on a state-wide

basis, three distinct groupings can be seen, corresponding to the arcuate

strand, cuspate delta and barrier island zones. It is felt that the sediment

types reflect three different sources of beach material. There is presently

no direct source of fluvial sediments on the arcuate strand, although several

rivers emptied into the ocean in this area during the relatively recent geo-

21
logic past While some sediment is being transported alongshore into the

area, most beach sands on the arcuate strand are apparently derived from an-

cient deposits lying directly behind the shore, as the area continues to erode.

Sediment samples from the arcuate strand show a wide range of size and sorting

values.

The cuspate delta area sediments are supplied by the Santee River, and

since the cuspate delta lies near its fluvial source, sediment samples from

the area are generally coarser than those found elsewhere on the coast. Due

to proximity to their source, the sediments are "immature", showing a wide

range of size and sorting Values.

The barrier islands of the central and southern portions of the coast

are farther removed from their fluvial sediment sources and are presently re-

ceiving very little sand. Sediments from this area have undergone a great

deal of reworking and, hence, are much better sorted than sediments to the

north. Due to lower wave energy in the area (and the constant reworking),

the sediments are significantly finer than those to the north. These fine-

grained sands pack very well, providing a hard pavement over which most motor

vehicles can easily drive.

COASTAL PROCESSES AND BEACH EROSION

Beach Erosion - An Overview

The erosion or accretion of any coastline is ultimately controlled by

the natural forces responsible for the movement of wind and water along the

beach and in the nearshore zone. Under the action of nearshore currents,

waves or winds, sediments are moved on, off and along the beaches. This

mass transport of sand on the coast results in the net erosion or accretion

14
of a particular segment of the coastline.

The erosion occurring along South Carolina's beaches is not unique to

this area. It has been estimated that there exists an average U.S. shoreline

erosion rate, due to natural causes (wave energy, gradual sea-level rise,
etc.), of between 1 ft. (30 cm) and 3 ft. (1 m per year 5. The National

Shoreline Study, conducted by the U.S. Army Corps of Engineers, concluded

that there are 20,000 miles (32,000 km) of eroding shoreline in the United

States, nearly 3,000 (4,800 km) of which are classified as critically erod-

ing areas (Table 1). These are areas where an erosion abatement program would

be justified for "economic reasons". According to their figures, nearly 43%

of the coastline of the U.S, is undergoing significant erosion. To consider

the causes of erosion on South Carolina beaches, it is necessary to understand

some of the basic causes of beach erosion in general. For purposes of communi-

cation, let us first consider some terminology. A typical beach is shown dia-

gramatically in Figure 9. This diagram appeared in the U.S. Army, Corps of

Engineers' Shore Protection Manual and was intended to represent a cross-section

of "typical" U.S. beaches. Anyone who has visited the South Carolina coast, how-

ever, should be quick to realize that this does not look like many 0f the

beaches in South Carolina.

However, Fig. 10 shows beach profiles that more adequately represent South

Carolina beaches even though they were measured on the Massachusetts coast. In

general, South Carolina beaches are wider and lower than many other beaches in

the U.S. This is primarily related to the large tidal range and the fine grain

size of the beach sands along the South Carolina coast. The upper profile in

Fig* 10 is the more frequently occurring constructional type. T "e two lower

ones display a more mature profile (10 September 1967) and the same station

after a brief summer storm (22 June 1967). Figure 11 displays four beach pro-

files that are representative of the morphologic provinces along the South

Carolina coast. Those profiles representing the more erosive portions of

the coast, the transgressive barrier (D) and cuspate delta (B) have steep

beach faces, probably because of the coarseness of the beach sediment. Pro-

file C is a beach-ridge barrier (Fig. 11) and resembles the constructional

beach profile at the top of Figure 10, reflecting the barrier's depositional

nature. The representative profile of the arcuate strand (Fig. 11A) is con-

cave upward, which is typical of.an erosional type beach profile.

Table I Shorelinc Charactcristics
Shoreline Shore Change Shoreline
Region Total Exposed Sheltered Eroding Non-Eroding With Without
Beac Beach
(miles) (miles) (miles) (miles) (miles) (miles) (miles)

North 8,620 4,730 3,890 7,460 1,160 2,320 6,300
Atlantic

South 14,620 2,470 12,150, 2,820 11,800 3,600 11,020
Atlantic-
Gulf

Lower 1,940 810 1,130 1,580 360 830 1,110
Mississippi
Texas Gulf 2,500 370 2,130 360 2,140 380 2,120

Great Lakes 3,680 3,020 660 1,260 2,420 2,110 1,570
Cal.ifornia 1,810 1,320 490 1,550 260 680 1,130
North 2,840 650 2,190 260 2,580 2,050 790
Pacific
Hawaii 930 900 1 30 1 110 820 180 750
Total 36,940 14,270 22,670 15,400 21,540 12,150 24,790

Alaska 47,300 20,20 27,050 5,100 42,200 Unknown Unknown

Total 84,240 34,520 49,720 20,500 63,740 12,150 24,790
National I I- I I I
From: -Report on National Shoreline Study, Department of the Army, Corps of Engineers, August 1971.

Coast .4 Beach or shore Neorshofs zon
defines area of nearshors currents)

Backshors rsshor% Inshore or shoreface --Offshore
- extends Wough breaker zone

Surf Zone

Berms
or men,

Beach scar, Breakers
Croot of berm HIgh water Is OL

Ordingry low water level

Plunge poInt
Bottom

Figure 9. Idealized beach profile displaying the features which may
be found in a "typical" beach cross-section (Shore Protection Manu-
al; Fig. 1-1).

DUNE RIDGE TYPICAL MESOTIDAL BEACH PROFILE

BERM RUNNEL RIDGE LOW-TIDE
TERRACE

MLW

10 SEPT 1967

3
22 juNE 1967 MLW

0 15 [email protected]

30 60 90 120m

Figure 10. Typical mesotidal (2-4 m tidal.range) beach profiles (MLW
mean low water). The upper profile is the more frequently occurring
constructional type.

4.00-B. CR03
4.00- A. 1230
20/7/75
,,140-4ER LHTS
LCB1 0.00- RACE )K
0.00- 0 FA WL
z 10/6/75

> LHTS -4.00-
LU
lu 4.00

CUSPATE DELTA
-8.00i
ARCUATE STRAND 0.00 20.00 4d.00 6d.()o 80.00
.8.00- 1 ___ I
0.00 20.00 4d.00 60.00 8d.00
DISTANCE (MI

4.
4.00- C. FB03 0 0- D. EBOI
1213 1329
8/8/76 0.00- 6/6/75
0.00-/ XLHTS LHTS
z WL
0
S RIDGE
< RUNNEL
> -4.00
Ui .4.06- xWL
LU
BEACH-RIDGE BARRIER -8.00 TRANSGRESSIVE BARRIER
-8.00- 26.00 0,00 2d.00 4d.00 615.00
0.00 40'00 6d.00 8d.00 10d.00 126.00 140.00 166.00
DISTANCE (M)

Figure 11. Beach profiles for representative stations from the four morphological provinces of
the South Carolina coast. (WL = water line at the time the profile was taken; LHTS.= last high
tide swash).

Causes of Beach Erosion

Wave attack. - In South Carolina, as elsewhere in the U. S., the primary

cause of beach erosion is wave attack. This is obvious to anyone who has stood

on or near the beach during a passing storm. What is often not so obvious is

the effect of smaller waves. During a minor storm in 1977 at Debidue Island,

up to 10 ft. (3 m) of shoreline eroded away in only a six-hour period. The

22
maximum recorded wave height associated with this storm was only 4 ft. (120 cm)

It should be realized that a catastrophe is not necessary to produce the rates

of erosion cited in the following pages; however, storm waves, no doubt, play

an important role in changing our shoreline (Fig. 12).

Research into what type of waves cause coastal changes has found that,

in general, short, steep waves tend to erode the beach while longer, lower

profile waves cause sand to be added to the beach. Four types of waves shown

in Figs. 13-16 occur on the S. C. coast. These are:

A) Spilling (Fig. 13): Bubbles and turbulent water spill down front face

of wave. The upper portion of the front of the wave may become vertical be-

fore breaking. Breaking is generally over quite a distance.

B) Plunging (Fig. 14): Crest curls over an air pocket; breaking is usually

with a crash followed by a smooth splash-up.

C) Collapsing (Fig. 15): Breaking occurs over lower half of wave. There

is no associated air pocket and usually no splash-up. Bubbles and foam are

present.

D) Surging (Fig. 16): Wave peaks up, but bottom rushes forward from under

wave, and wave slides up from beach face with little or no bubble production.

Wave type plays a major role in determining the severity of erosion.

Plunging waves tend to suspend large amounts of sand in the water and, there-
fore, are the most erosive type of wave along the beach. 23

The seasonal variations in wind and wave conditions along the S. C. coast

were noted in the diagrams displayed in Figures 2 and 3. The dominant winds

Dune Crest

Ile,m

M H. W._
Profile A Normal wove action

M'[email protected]'

M.H W.
-N,
Profile B - initial attack of
storm waves M.L.W.

ACCRETION

Pro file A

!Storm Tide
E R 0 S 1 0 N M H, W.

Crest
Lowering Profile C Storm, aye attack
of I w M.L W
or dune
Cr est
1 R ec ession ACCRET ION
Profile A

0 M WW

M,L,W.
Profile D After storm wave attack,
normal wove action
ACCRETION

Profile A

Figure 12. Schematic diagram of storm wave attack on coastal beaches
(Shore Protection Manual, Fig. 1-7).
E 7R N
0 S 1 0
[email protected]
.file C fojrr'w a v e t t a c
u
d

I-

.... . . . . . . . . .

... .. . .

Figure 13. Spilling breaking wave.

[email protected],

Figure 14. Plunging breaking wave.

Figure 15. Collapsing breaking wave.

11 P't

Figure 16. Surging breaking wave.

(highest velocities) from the north and east during fall and winter (Fig. 2)

are reflected in the direction of the deep water wave energy (Fig. 3). Strong

storm winds from the northeast are generated by northward passing extratropical

storms and are considered to be the most important wave generators on the South

Carolina coast. Up to 24 ft. (7.3 m) of foredune erosion was documented on

Debidue Island in a two-wdek period following an extratropical cyclone in

February 1973 . In spring and summer, an increasing frequency of winds are

observed from the south and southwest. These winds are generated by an anti-

cyclonic circulation pattern associated with a high pressure zone settling over

Bermuda.

Storm surge. - Storm surge is a rise above normal water level on the open

ocean along the coast due to the action of wind stress on the water surface.

During a hurricane, storm surge is accentuated as a result of reduction

in the atmospheric pressure. Storm surge is the primary agent of geo-

logic change in storms, particularly hurricanes. The generation of storm

surges gives hurricanes the ability to pile up great quantities of water

10
against the coastline The storm surge is determined by the effect of wind

velocities in the hurricanes, by the speed of its forward movement, and also
by the offshore bathymetry 32

Storm surges can produce extremely high tides along the South Carolina.

coast, flooding areas along the coastline that lie above mean high tide. Strong

winds producing high waves in conjunction with a storm surge tide can cause

severe beach erosion along the coast. Table 2 provide some storm surge tide

levels for Charleston, South Carolina.

Hurricanes. - Two general categories of storms strike the'coastal region

of South Carolina. These are: tropical storms or hurricanes, and extratropical

storms, commonly referred to as.northeasters. Although hurricanes are by far

Table 2. Storm surge tidal elevations affecting Charleston, S. C.
(1893-1964) (From Myers, 1975).

Storm Date Maximum Storm Tide (Ft)

28 Aug. 1893 8.9
11 Aug. 1940 8.0
27/28 Aug. 1911 7.9
27/28 [email protected] 7.0
29 Sept. 1959 (Gracie) 6.0
15 Oct. 1947 6.0
14 July 1916 5.9
20 Oct* 1944 5.8
18 Sept. 1928 5.6
17 Aug. 1955 (Diane) 5.2
11 Sept. 1960 (Donna) 5.0
18/19 Sept. 1955 (Ione) 4.4
11 Aug. 1955 (Connie) 4.3
15 Oct. 1954 (Hazel) 4.2
29/30 Aug. 1954 (Carol) 4.2
30 Aug. 1952 (Able) 4.0
27 Sept. 1958 (Helene) 3.9
25 Oct. 1963 (Ginny) 6.9

the more severe storms, their lower rates of occurrence make them less signifi-

cant than northeasters in terms of continual shoreline change. The probability

of a hurricane-force tropical storm striking the South Carolina coast is about

0.04, or one in every 25 years (Table 3). The effects of northeasters along

the South Carolina coast as a cause of beach erosion is discussed in the pre-

vious section on wave attack.

Hurricanes are storms of tropical origin with a cyclonic wind cir culation

(counterclockwise in the Northern Hemisphere) of 74 mph (64 kts) or higher.

'Hurricanes occur in the North Atlantic with a frequency of approximately 7.5

per year and occur most often during the months of August, September and Octo-
ber 6. The name "hurricane" is derived, via Spanish, from a West Indian word
27
for the storms Over the years, hurricanes have produced many disasters

alo ng the South Carolina coast. The loss of life and damage to property by

these storms is primarily the result of the hurricane storm tide (discussed

earlier as "storm surge") and, on the immediate coast, high waves. The hurri-

cane winds are also a danger. The more destructive hurricanes of the past

Aug. 1893

".."4 Aug. 1885
C) Aug. 1881

C-4
660

Figure 17. Tracks of the major late 19th century hurricanes affecting the
South Carolina coast (from Myers, 1975).

Aug. 1911

0 Sept.-
20 Oct. 1959
1, Aug. 1940

7 0

0
a t.
HAZEL
Oct. 1954 0

Figure 18. Tracks of the damaging hurricanes of the 20th century affecting
the South Carolina coast (from Myers, 1975).

vividly illustrate the potential danger of life and property along the South

Carolina coast. The storm tracks of those hurricanes which had a damaging

effect on the South Carolina coastline are displayed in Fig. 17 (for the late

19th century) and Fig. 18 (20th century).

One of the most severe hurricanes to strike the South Carolina coast

was hurricane Hazel in 1954. The storm track of this hurricane is shown in

Figure 18. A description of its destructive path along the South Carolina

shoreline is given below.

"Hurricane Hazel entered the coast just north of Myrtle Beach, S. C., and
was one of the most destructive hurricanes, in terms of property damage. Hur-
ricane winds hit the Atlantic Coast between Georgetown, S. C., and Cape Look-
out, N. C., and storm tides devastated the immediate ocean front of this stretch
coast. Every fishing pier from Myrtle Beach to Cedar Creek, N. C., a distance
of 170 mi., was destroyed. High tides of 16.6 MSL were observed at Holden
Beach Bridge and Calabash, N. C. The lowest recorded barometric pressure of
938 mb was reported at Little River Inlet on the South Carolina-North Carolina
border. At Cherry Grove Beach., a 17-ft MSL tide destroyed all front-row houses
and washed some second-row houses from their foundations. At Tilghman Beach,
Ocean Drive, Crescent Beach, Atlantic Beach, and Windy Hill, S. C., practically
all front-row houses were destroyed or damaged, with waves breaking at house-
top heights along some of the beach front. At Myrtle Beach, high-water marks
at "Edgewater Apartments" near 16th Avenue South indicated a tide height of
15.5 ft MSL. The highest wind gust at Myrtle Beach AFB was 106 mph. It is
estimated that wind and water combined badly damaged or destroyed about 80
percent of the beach front property in the Myrtle Beach area. At Surfside
and Garden City, S. C., hundreds of houses were destroyed by tides in excess
of 13 ft MSL. On Pawleys Island, S. C., 75 percent of the houses on the beach
were badly damaged, and 10 ft waves covered.the northern and southern ends of
the island, as well as low-lying areas in the middle. At Georgetown, sections
of the streets were inundated. Folly Island, Sullivans Island and isle of
Palms suffered light property damage and slight beach erosion. No serious
damage was done at Charleston. Total property damage was estimated at $34
million in North Carolina, $27 million in South Carolina. Advance warnings
enabled people to evacuate the threatened areas, and only one person was
killed in South Carolina as a result of this storm. After devastating the
coast, hurricane Hazel moved across North Carolina with diminishing winds,
passing through Virginia and heading northward toward Lake Ontario and
Canada" (Corps of Engineers, 1957) (From Myers, 1975).

Sea level rise. - One of the most important yet least obvious geologic

agents of shoreline erosion is the slowly rising level of the sea. While

rapid erosion may take place during storms as beaches suffer from wave attack,

a longer term shoreline erosion resulting in barrier island retreat is the

result of a relative rise in sea level (Fig. 19). Sea level has been steadily

(INST CURE few ava,f
-,HOUSE IIWNPA IPIP-1
FIRST DUNE 1ftftV. wo,.)

FALLEN HQM ffW ".1
IwOONAL HIGH TME

WATER

PROFILE AFTER STORIO

PROFILE SEMNE STORIO

SHORT-TERM EROSION

try or CURE (CROSIONI
"0"

LEVELP"WILE BEFORE RISI IN SEA LEVEL
[email protected] NEAR SEA LEVEL

IRA 11 11
PINEV'OUS

LONG -TERM MIGRATION

From Pilkey and ottvers,1975

Figure 19. Beach and dune changes resulting from storms and the relative
rise of sea level (from Pilkey et al., 1975)

TIME (years)
1920 1930 1940 1950 1960 1970

15
CHARLESTON, S.C.
E

-10

-5

FORT PULASKI, GA.

Figure 20. Changes in sea level with respect to the adjacent land at
F"
T
L7=

m ERO=N
0 @[email protected]

Charleston, S. C. and Fort Pulaski, Ga. (from Hicks and Crosby, 1974).

rising since the end of the last glacial epoch, approximately 14,000 to 18,000

years before present (years BP). Between 14,000 and 7,000 years BP, the sea

rapidly rose, and the shoreline retreated some 50 miles from the edge of the

28
continental shelf . From 7,000 to approximately 3,0 00 BP, sea level along
the east coast of the U.S. rose at a rate of about one foot per century 25 .

The sea level curve for the Delmarva Peninsula shows a relative rate of sea

level rise of approximately half a foot per century for the past 3,000 years.

Although sea level has been continuing to rise, it is doing so at an ever

decreasing rate. However, between 1964 and 1971, sea level rose 4 inches
(10 cm) along many portions of the east coast (Fig. 20) 16. The recent and

relatively rapid rate in sea level rise of roughly half a foot per decade is

probably only a short term fluctuation, but striking nonetheless.

EROSION-DEPOSITION TRENDS

The causes of beach erosion have been outlined above. A final considera-

tion is how does the beach build after an erosive event. After a storm, the

beach is wide and flat and often backed by a scarp (Fig. 21). The sand that

was removed from the beach is deposited offshore as a bar. Soon after the

storm (usually 2 days to 6 weeks), small ridges of sand migrate onto the beach

and gradually build a low berm (Fig. 22). This feature is further built by

waves rushing up the beachface and over the berm top where sand is deposited

Finally, wind-blown sediments are trapped by straw and debris deposited above

high water level and form low, incipient dunes. If left alone, these will

develop a mature dune ridge. In essence, the dunes become a type of natural

levee against wave attack providing a line of protection from storms and serve

as a reservoir of beach sand.

Z
'7

-f :"ZM

7,
v-1

S.
I MGM

7,
'R
'R,

Figure 21. Typical post-storm (1 day) beach profile displaying a wide, flat
beach backed by a scarp.

Ng,n,

Ng ZI �N'k "Z""PI",
g "

-OWN

7
-M
7z
MM

Figure 22. Profile at the beach two to six days after a storm which shows the
development of a low berm. Photo taken at Kiawah Island, S. C.

The cycle of erosion and deposition on beaches differs markedly from

place to place and is dependent on such variables as:

1) direction of prevailing winds

2) sand grain size

3) nature of stormactivity

4) wave climate

5) nature of offshore topography

A series of beach profiles displaying trends of erosion and deposition

over a 2-year period for each of the four morphologic provinces of the South

Carolina coast is shown in Fig. 23. The migrating beach ridges in the pro-

files from Hilton Head Island represent a form of sediment accumulation in

the coastal zone, while the steep beachface and extended washover terraces

of Cape Romain are erosive beach features. A very important reservoir of

sand along the South Carolina coast is the large ebb-tidal deltas associated

with the seaward projection of tidal inlets. These shoals contain large vol-

umes of sediment and are an important source of sand for the accretion of

beaches along portions of the South Carolina coast (Fig. 24).

Certain generalizations are possible regarding the overall trends of

erosion and deposition along the South Carolina coastline. Depositional

trends are most likely to occur at the downdrift ends of barrier islands.

Although drift reversals do occur, over most of South Carolina the trend of

longshore sediment transport is to the south. Deposition occurs as sediment

in recurved spits is welded to the shoreline as spits successively migrate

southward. At Cape Romain, recurved spits have prograded in two opposite

directions because of the unusual shoreline orientations at the Cape (Fig. 7).

Erosional areas are related to several factors. At Cape Romain, Rac-

coon Key, Morris Island and Edingsville Beach, extensive erosion is taking

MYRTLE BEACH HILTON HEAD

PWOI is HH15
,/DUNE 31/ 7/74-19/8/76

MIGRATING RIDGES

'Arcuate St and '113each-Ridge Barrier
o -
0. cc 20. 03 '0 . C.50 cc loc. 00 !,20. cc 00 20. 00 LlO. 00 60.00 M 00 100.00 120. 00
T 'l N C F 015 TRNCE @Ml l4o. oa i6c. all

,7 CAPE ROMAIN EDINGSVILLE BEACH

-Rol EBO I

WASHOVER TERRACE
BEACH FACE

Transgressive Barrier
Cuspate Delta
[email protected] 20. Do @0.00 50 00 M 20
DIS'ANCE (M) 00 Go t 20 - 00 [email protected] 21. 60. Do 63.00 100.00 "20.00 "o.oo 160.00
DISTPNCE M1

,j'igure 23. A series of beach profiles (sweep zone) displaying trends of
erosion and deposition over a two-year period for each of the morphologic
provinces of the South Carolina coast.

IQLOO

00 M3
69,000,0
STONO
6M
EBB
cr
JIDAL
DELTA

SEDIMENT VOLUMES
KIAWAH-SEABROOK 252,000,000 3
128,000,000 BARRIER ISLAND
EDISTO EDISTO-STONO 197,000,000 M3
EBB-TIDAL EBB-TIDAL DELTAS
DELTA -
DIFFERENCE 55,000,000

3 0 5
t .
r

Figure 24. Volumes of sand contained in Kiawah and Seabrook Islands and the
ebb-tidal deltas of the two adjacent inlets, Stono and North Edisto (from
Hayes et al., 1976) 32

place along marsh shorelines. Erosion at the Santee D elta, Cape Romain, and on

Morris Island can be related to the reduction of sediment supply resulting from

artificial controls due to modifications by man. In other areas., the erosion is

related to the fact that the beaches are exposed to severe wave attack from

large stretches of open water. This is true for northern Bull Island, Cape Ro-

main, and the southern tip of Edisto Beach.

Without exception, highly unstable areas are related to the presence of tid-

al inlets. Lateral migration of inlets, wave refraction around inlet-associated

shoals and changes in inlet morphology all cause rapid and large-scale erosional-

depositional fluc tuations in areas associated with inlets (Fig. 25). In places,

such as at Bull Island, these effects can modify the beaches up to two miles

away from the inlet.

Stable shorelines occur along the central por tions of the larger islands.

These beaches are far away from tidal inlets. Also, some stable areas are the

result of large monetary expenditures to construct groins and seawalls to hold

the sand in place and prevent movement of the shoreline position (Fig. 26). ,

Recently, a computer program has been developed that can predict wave re.7

fraction patterns and the resulting distribution of wave energy along the South

Carolina coast (Fig. 27). These results have proven useful for' determining

zones of potential erosion or deposition along the coastline. Some of the more

interesting findings include:

1) The 11yrtle Beach area, or the South Carolina "Grand Strand", appears rela-

tively protected against damage by a northeast storm. However, the most vio-

lent storms known to hit the state, the hurricanesi may actually focus wave

energy on this highly developed shoreline section.

2) In a manner similar to Myrtle Beach, the southwestern part of the Isle of

Palms appears relatively protected against northeast storms but very exposed

to hurricane waves arriving from the south or southeast.

Figure 25. Morris Island light. The lighthouse was located on the beach at
the south end of Morris Island in 1939. Over 1600 feet of erosion has oc-
curred since that date. This erosion is in part related to the construction
of jetties at Charleston Harbor to the north, as well as its proximity to a
tidal inlet. Photo taken January 7, 1975.

J
"M

Figure 26. Oblique aerial photograph of a series of gr oins constructed along
Edisto Island beach. Note the accumulation of sand along the updrift
(eastern) margin of each groin.

M, M M M Olin M ow M M M

ovl-
t N *0 \[email protected]

@,ZT 10-

A,\ [email protected]

Figure 27. Computerized wave refraction diagram for waves of 10 sec. period out of the east. This
diagram shows the effects of northeasters on the South Carolina coastline. Each line intersecting
the coast represents the approach of a series of wind-produced waves (from Fico, 1977).

3) The large downdrift offset of Dewees Inlet appears to be related to a sudden

reduction in southward-directed longshore drift at the Isle of Palms compared to
Dewees Island and the other barriers further to the north 8

SHORT TERM CHANGES

This next section examines the short-term erosion-deposition trends for

the four major morphological provinces along the South Carolina coastline. This

section is preceded by a discussion of how and what kind of data was collected

for this study.

What is a beach profile?

A beach profile is a topographic survey run normal to the trend of the

beach. Profile locations were selected after careful aerial and ground recon-

naissance of the entire coast of South Carolina. At each site, two permanent

reference stakes were set well landward of the spring high tide position on a

line normal to the beach. The top of either stake served as a permanent ori-

gin for all beach profiles run at that location. The surveying technique is
modified slightly from the method illustrated in Figure 28 7

Data Presentation

Since 1973, personnel from the Coastal Research Division have run well

over 1000 beach profiles along the South Carolina coast. The large volume

of data generated from these studies would be, at best, unmanageable if

treated by hand. Therefore, a program was created to reduce and store these

data in the University computer facility. These profiles can be recalled

singly or as a group and plotted in one of three formats.

In later sections of this report, information on moderate to long-term

changes in beach configuration will be discussed. Although these types of

information are extremely useful for the coastal zone planner, it is neces-

sary to consider the shorter term (monthly or seasonal) variations that can

be superimposed on these longer trends. It is only at this scale that we

2
7-

5
. ... . ......

er
. . . . . . . . . .

Figure 28. Photograph illustrating the survey technique of Emery
(1961) used to determine beach profiles.

BEACH PROFILE CHANGES
KIAWAH ISLAND, S.C.

KW 10

8 JUNE 74
KW5
8 MAY 75 EROSION
.... . ....... DEPOSITION

..........................
KW I

............. ------------------
--- 9JUNE 74
8 MAY 75

....................
-21 JULY 74
8 MAY 75

0 100
........ .
...........

Figure 29. Beach profile changes at 3 stations, KW-1, KW-5, and KW-10
between June-July 1974 and May 1975. 'Station KW-1, located near the
Guest House on Seabrook Island showed the most erosion of any station
(over 100 m of landward retreat of the high tide line). Station KW-10,
which is located on the lee side of a large offshore sand shoal, showed
the largest amount of accretion (over 100 m of seaward progradation of
the high-tide line). Station KW-5, located in the middle of Kiawah,
showed little change (from Hayes, 1977).

can fully understand the relationship between coastal processes and beach changes.

For that reason, the South Carolina Beach Profile Network was established.

This network consists of approximately 70 beach profiles. Thirty-five

of these profiles were run at one month intervals for two years to establish

the pattern of short-term changes associated with each location. They are

presently run at 3-month intervals to document seasonal erosion-deposition

patterns along the South Carolina coast. In addition, 35 profiles have been

surveyed at varying intervals as part of other Coastal. Research Division pro-

jects.

First, individual profiles can be plotted separately. Each plot shows

the beach configuration.for the days on which beach profiles were run. In

addition, any two profiles at one station can be overplotted to show changes

in the beach between surveys. The amount of change is calculated and is dis-

played as the area between the two profiles (Fig. 29). This information can

be used to determine the response of different beaches to a variety of events

(storms, long periods of fair weather, etc.). Finally, all of the surveys

from any one location can be overplotted to define a sweep zone (Fig. 23).

By superimposing all the data from one profile in this fashion, we can readily

see the maximum and minimum elevation of any point along the beach profile and

determine the variability (or lack of it) that has occurred during that period

of record.

To facilitate discussion and conserve space, the profiles will be con-

sidered in groups rather than individually. Complete data listings for in-

dividual profiles can be obtained by writing to:

Coastal Research Division
Geology Department
University of South Carolina
Columbia, S. C. 29208

The areas discussed are 1) the grand strand, 2) the North Inlet area, 3) Cape

Romain, 4) Capers and Bull Islands, 5) Sullivans Island, 6) Isle of Palms,

7) Folly Beach, 8) Kiawah Island, 9) Edisto Beach, 10) Hunting Island, 11)

Fripp Island, and 12) Hilton Head Island, for short term changes.

Grand Strand

The grand strand (Fig. 30) is 50 miles (80 km) of straight to gently-

curving shoreline. The beaches of this area are characteristically wide and

flat. Beach profiles in this area reflect general shoreline stability, which

is in agreement with longer-term information. Most of the moderate variability

seen in this area is roughly seasonal, and net changes through the study period

were small.

The nature of the backshore area varies from profile to profile. At sta-
tion CGB-1, a we'll-developed dune system of over 10 feet high sits in front of the first

row of houses as protection against sudden erosion (Fig. 31). Likewise, at

station LCB-1, substantial foredune ridges occur locally. These dunes are well

vegetated, primarily by sea oats (Uniola peniculata). At the beginning of the

study period, a 6 ft. (2 m) dune ridge was present at station NMB-2. This ridge

was subsequently removed, presumably for development purposes, and the profile

is presently backed by a high-rise condominium (Fig. 32).

Debidue and North Islands

At the southern end of the grand strand is the Belle W. Baruch Plantation.

Contained within the tract are two Holocene barriers, Debidue and North Islands,

separated by North Inlet (Fig. 33). In the vicinity of the inlet, the barriers

are wide. Further from the inlet (to the north and south), the islands thin

to approximately 1000 ft. (300 m). On North Island, a low and continuous dune

ridge partitions the marsh from a wide supratidal flat. In contrast, actively

eroding foredune scarps (4-6 ft. high) and washover deposits dominate on Debidue.

Both beaches are wide and relatively flat, while seasonal variations are minimal.

Both Debidue and North Islands are characterized by instability. Exposure

of Spartina alterniflora peat occurs on the lower foreshore at both beaches.

@4g

Figure 30. Oblique aerial view of the arcuate strand looking north
from Murrells Inlet.(from Brown, 1977).

ga,

7
@v:

Figure 31. Well-developed dune system in front of the first row
.,of.,houses.,at station CGB-l, Garden City beach. These dunes
provide protection from storm-p'roduced wave attack.,

ft%r

SUN%&
NOUN 77, ,Z

@.... .... . . .
[email protected]
. .... OOOOM

J.
@,q

Figure 32. Location of profile station NMB-2 at North Myrtle Beach..
The higl--i-rise condominium presently backs the profile.

Figure'3a. Oblique aerial view of North Inlet that separates Debidue
(to the north) and North Islands.

oe @ e7-1 -

Figure 34. Aerial photograph of Cape Romain. Sediment eroded from the
cape moves away in two directions forming recurved spits to the north
and west.

42 M

Historic charts show southward inlet migration by recurved spit accumulation

and shoreline retreat in the vicinity of the inlet. Seasonal profile data shows

that Debidue Island is more stable than North Island.

Cape Romain

Cape Romain is a large cuspate foreland. This area is quite unstable and

presently migrates landward at a rapid rate. Sediment eroded from the vicinity

of the Cape moves away in two directions forming recurved spits to the north

and to the west (Fig. 34). Beach profiles in this area reflect a general shore-

line instability. The Cape is dominated by beach erosion and wa shover deposi-

tion. A steep beachface and extensive washover terraces are typical for much

of the central portion of Cape Romain.

Capers-Bull Islands

Overall, these beaches are generall quite wide (235 ft. at Bull; 240 ft.

at Capers) and relatively flat; however, the beaches adjacent to Price Inlet

(Fig. 37) are even wider and are the sites of frequent ridge-and-runnel sys-

tems. These profiles have been generally stable and are backed by small in-

cipient dunes covered by sea oats (Uniola peniculata) or sparse maritime

forest.

Further from the inlet, the profiles exhibit much more variability. Sta-

tion BUL-1, on central Bull Island, has been erosional throughout the study

period. At station CI-02, on Capers Island, although net changes have been

small, drastic changes in beach position and configuration can occur, evi-

denced by the high scarp and the in-place palmetto trees on the beach (Fig. 36).

Isle of Palms

Beaches at the Isle of Palms generally increase in width from 150 ft. at

the northern end to 325 ft. at the southern end. With little exception, the

entire length of beach is backed by dunes. At profile IP-01, on the northern

end of the island, the dunes are small (approximately 2.5 ft.) and sparsely

[email protected]

Figure 35. Aerial photograph of Price Inlet and the adjacent beaches of
Bull and Capers (view is to the south).

W.-
&

4!.

!4
".4%
4,7

A
N

106
V

Figure 36. Ground view of profile station CI-02 on Capers Island. Drastic
changes in beach configuration are evidenced by the occurrence of a high
scarp and in place palmetto trees.

vegetated, A small scarp often occurs due to wave attack, At IP-02, the dunes

are still small, but they are wider and better vegetated with sea oats (Uniola).

Further south, at profile stations IP-03 and IP-04, dune height increases to

5 ft. (1. 5 m) .

Effects of development can be seen at all profile locations. IP-01 sits

in a grain field and is backed by front row houses. At IP-03 and IP-04, the

second row of dunes was leveled for development purposes (Fig. 37).

The beaches along Isle of Palms have generally been stable. With the ex-

ception of station IP-04, little change in the position of the beach was noted

through the study period.

Sullivans Island

All beach profiles on Sullivan's Island are extremely wide, averaging

over 500 ft. (152 m). Ridge-and-runnel systems are common at stations SI-00

and SI-01. Dune height varies between 2.5 and 6.5 ft. Dunes are vegetated

by sea oats (Uniola) and at SI-02, by wax myrtle.

Folly Beach

Beaches in this area are characteristically wide (260 ft.) and flat. In

general, dune height increases in a southerly direction. At station FB-01,

the beach is backed by overwash and small incipient dunes. At FB-02, dunes

vary between 3 and 6 ft. in height and are vegetated by sea oats (Uniola).

Houses are built in or on the edge of the dune field. The largest dunes on

the island occur at FB-03. Heights up to 15 ft. (4.5 m) were measured. De-

velopment is confined to a small road through the back of the dune field.

The erosional-depositional trends along Folly Beach are highly variable.

Slight net erosion was measured at FB-01 through the study period. At FB-02,

slight accretion occurred. Exact determination of erosion-deposition rates

at station FB-03 are impossible. In almost every instance, the permanent pro-

file stakes were either removed or eroded away between surveys.

N it

77
iq

Figure 37. South end of isle of Palms. Southerly migration of
Breach Inlet has allowed the deposition of a recurved spit at
the south end of the Isle of Palms. Note houses built on older
recurves. Large open area is where a developer has flattened
the sand dunes in the location of profile stations IP-03 and IP-
04. View looks north.

Kiawah Island

Kiawah Island is composed of a series of prograding beach ridges that have

been highly modified on either end by migration of adjacent tidal inlets. In

the central portion of the island, the beach is wide (80 - 300 ft.) and flat.

The dune area in this part of Kiawah is also relatively wide, averaging between

250 - 300 ft. (75 - 90 m). There is usually a well-defined foredune ridge that

rises 5 - 10 ft. (1.5-3 m) above the swash line of high spring tides. In most

of this area, there is also an intermediate high dune ridge as well as a high

dune ridge at the back portion of the grass vegetation. The vegetation in the

dunes is dominated by Uniola (sea oats), Iva imbricata (sea elder) and Croton

A three-dimensional block diagram of a segment of this zone is given in Figure

38. Further to the east is an area characterized by progradation. The beach

in this area is wide, averaging about 425 - 460 ft. (130 - 140 m) and is charac-

terized by consistently larger depositional features than those found in the mid-

barrier straight beach. Well-developed ridge-and-runnel systems are common in

this area. The backshore is highly complex and extremely wide, reaching a maxi-

mum width of approximately 4.3 miles (2.7 km). The beach ridges are quite high

in places, commonly attaining heights of 10-15 ft (3-4 m)., They are often

separated by expanses of salt marsh averaging approximately 650 ft (200 m) in

width. Many tidal creeks are located between the beach ridges, and, in some

places, the meanders of the creeks cut into the ridges. Generally, the beach

ridges are covered with climax forests dominated by live oaks and palmettos,

but there are a few that have pine forests of unknown origin.

Near the eastern end of Kiawah Island, the beach is frequently overwashed

during high spring tides and storms. The intertidal beach in this area is

relatively complex, ranging in width from approximately 60 ft. to over 200 ft.

In places, the beach is steep and undergoes some dramatic seasonal changes, with

ridge-and-runnel systems and well-developed low-tide terraces having been ob-

served during the summer months. The opening and closing of the two small

tidal inlets that occur in the area bring about changes in the profile, such

as the development of small tidal deltas at the mouths of the creeks. The

most conspicuous features of the intertidal zone are the large outcrops of

peat and intertidal muds. These deposits commonly contain abundant razor clams

and oysters in life position, all of which are less than 50 years old. There

is no recent dune area along this stretch of the beach. The washover terraces

and fans are building into a salt marsh dominated by Spartina alterniflora

(smooth cordgrass) and Spartina patens (salt-meadow cordgrass). The supratidal

sand areas contain abundant Salsola kali (Russian thistle) and other dune vege-

tation. The washover terraces average 65 98 ft. (20 - 30 m) in width and

have flat to slightly landward dipping surfaces that are littered with shell

and heavy mineral accumulations, There are a few isolated wind-shadow dunes

which attain a height of 2-4 ft. (.6-1.2 m). This section of the beach con-

tains an unusually large percentage of heavy minerals, presumably a result of

their concentration by waves as part of the erosional process. A unique as-

pect of this area is the fact that the beach zone can be intensely eroded by

runoff of rain water. During heavy rains, water will accumulate behind the

washover terraces and the low foredune ridges. As this water eventually break s

through these natural dams and spills down the beach front, large erosional rills

and channels are developed.

The west end of the island is a recurved spit complex associated with

Kiawah Inlet. This-spit is 1.7 miles (2.1 km) in length and has a maximum

width of 2000 ft. (Fig. 39). The growth of the spit present today was ini-

tiated around 1949. In terms of its morphology, the spit is made up of es-

sentially two zones: a) recurved, vegetated dunes, and b) the intertidal

beach zone. The intertidal beach zone is wide and flat, averaging about

300-600 ft. in width. The beach profile normally contains two low-amplitude

DUNES ATLANTIC OCEAN
a
b

MTL

CLITORIA MARIANA
4- PANICUM AMARUM
STROPHOSTYLES HELVOLA
CYPERUS Sp.
QUERCUS WRGINIANA
OPUNTIA DRUMMONDII -A
ERIGERON CANADENSIS IL JL__j
OENOTHERA HUMIFUSA III
HETEROTHECA SUBAXILLARIS
GAURA ANGUSTIFOLIA
HYDROCOTYLE BONARIENSIS
SMILAX BONA-NOX
CENCHRUS TRIBULOIDES
UNIOLA PANICULATA
TRIPLASIS PURPURFA
CROTON PUNCTATUS
EUPHORBIA POLYGONIFOLIA
KIA 5

10 0 30
VERTICAL EXAGGERATION X5 METERS -
SCALE

Figure 38. Three-dimensional block diagram of a segment of the beach and dune
ridge environment of Kiawah Island. The transect extends from mean tide level
(14TS) across the foredune ridge (b) to the rear dunes (a). The diagram shows
the vegetation zonation for this section.of Kiawah Island-(from Hosier, 1-975).
a

ggm-
@17

.q,
q,

pp,

Figure 39. West end of Kiawah Island. The lateral Figure 40. Ground view of profile station
migration of Kiawah River has resulted in deposi- EB-01 at Edisto Beach showing the local
tion of this classic recurved spit. View looks to occurrence of shell beach ridges and.large
the north toward Kiawah Island. shell overwash deposits.

ridges on the seaward half of the profile. On several occasions, the inner

ridge welds to form a very low-amplitude berm. The dune ridges are distinctly

linear and curve in toward the Kiawah River. The ridges are continuous for

several hundreds of feet and attain a maximum height of approximately 10 ft.

(3 m) above the swash line of high spring tides. It is evident that the neck

of the spit has been overwashed by storm surges during the past decade. There-

fore, the highest dunes are found in the widest portion of the recurve. The

dunes are vegetated primarily by grasses with Uniola, Ivy, and Croton being

the most common forms. Spartina patens (salt-meadow cordgrass) and Spartina

alterniflora (smooth cordgrass) occupy the swales between the ridges on the

landward side of the spit.

Edisto Beach

Edisto Beach is generally narrow (100 - 125 ft.) and steep. It is largely

a transgressive or erosional type of barrier. Exposures of marsh peat on the

beachface at Edisto Island are not uncommon. The high contribution of shell

material in the sediment has resulted in a large grain size. Often, this

coarser material is concentrated in shell cusps on the beachface.

The character of the area backing the beach is highly variable. At EB-01,

shell.beach ridges occur locally (Fig. 40). Large shell overwash fans are

transgressing over active salt marsh. At station EB-02, the beach is backed by a

remnant maritime forest at the northern end of the public camping area. EB-03

is characterized by low dunes (3-5 ft.) backed by front row houses.

Beach profile data indicate that erosion of these beaches is largely re-

lated to storm activity. Station EB-01 showed net erosion throughout the study

period, most likely rela ted to the low elevation of the beach in this area. Sta-

tion EB-02, however, showed overall stability, and EB-03 demonstrated net accre-

tion. Therefore, the exposed marsh peat and other indications of a rapidly

eroding profile are sh ort-1 ived features. It should be stressed, however, that

although these areas show an overall stability or accretion, they have been

highly variable at times.

Hunting Island

Hunting Island is a state-owned park facility. Beaches in this area are

quite wide (about 300 ft.) and of intermediate steepness. The beaches are

backed by low dunes and, in the central portion of the island, maritime forest.

The highest variability measured in the area occurred at station HI-02 where

erosion of up to 8 ft. (2.5 m) between monthly surveys was measured in 1976.

Evidence of these rapid changes are the tree remains exposed in the present

beachface (Fig. 41).

Hunting Island has been the site of two beach nourishment projects. The

source for the first, in 1964, was a large borrow pit in the central portion

of the island. Sand for the more recent nourishment was obtained from the

shoals at the mouth of Fripp Inlet (Fig. 42).

Hilton Head Island

Hilton Head Island, South Carolina's development "jewel" is the site of

some of the most luxurious summer and year-round homes on the east coast. Is-

land beaches are characteristically wide (300 ft.) and of mode rate steepness.

The beaches are generally backed by some sort of dune ridge or dune system.

At HHI-2 (Fig. 43), a low, planted ridge covered by Uniola (sea oats) occurs.

At HHI-3, a 6 ft. (2 m) ridge was created artifically from coarse dredge

material. The back portion of the ridge is covered by low grasses, but the

face of the dune is bare and exposed to wave attack. Further north at HHI-04

(Fig. 44), a wide (3 ft.), high dune ridge is covered with a healthy growth

of Uniola. Other flora are scattered on the seaward edge of the dunes.

Generally, the beachfront on Hilton Head shows remarkable stability or

accretion. One notable exception occurs at station HHI-3 where slow, steady

erosion was measured throughout the study period. This area is not suffering

[email protected]

Figure 41. Tree remains exposed on the present beachface in the locality
of.station HI-02 at Hunting Island.

Figure 42. Aerial view of Fripp Inlet-showing the source of sand for
the more recent nourishment project on Hunting Island. The sand was
obtained from the shoals on the seaward side of Fripp Inlet, referred
to as [email protected] delta.

[email protected]

Un
-r-

'7777

I MAthfiRd

Figure 43. Ground view of profile station HHI-2 at Hilton Head Figure 44. Ground view of profile station
Island. The beach in this location is backed by a low planted HHI-04 at Hilton Head Island. Here,
ridge covered by Uniola (sea oats). there is a naturally occurring dune
ridge about 3 ft. (1 m) high also covered
by a growth of Uniola.

from erosion due to extreme waves or tidal currents. Instead, it is felt that

this sudden change in erosional character of the beach is related to the arti-

ficial shaping and molding of the beach. This practice is referred to as

beach "manicuring" and often creates more problems than it may immediately

solve.

LONG-TERM CHANGES

Up to now, this report has concentrated on the short-term variability and

erosion-deposition trends along the South Carolina coast. This information

is valuable in providing insights of the day-to-day changes on beaches and

barrier islands, as well as defining areas of general stability or instability.

However, it is most important to homeowners and coastal planners to examine the

longer-term variations in these areas. An important consideration in any beach

management program is the establishment of a reasonable set-back line, seaward

of which no construction is allowed. Critical to the determination of such a

line is the knowledge of the changes that can be expected along any given sec-

tion of beach through time. The individual erosion-deposition curves presented

in this section detail the variability that exists at given locations over the

past 25 to 50 years. Erosion-deposition data in this report could be used in

conjunction with existing environmental data (wave height, storm surge expec-

tance, etc.) to establish zones where development should be prohibited.

Study Procedure

Information appearing in the following section comes from two sources:

coastal charts and sequential vertical aerial photographs. Vertical aerial

photographs were obtained from the U.S. Agricultural Stabilization and Con-

servation Service, the United States Geological Survey and the National Archives.

Charts were obtained from the National Ocean Survey, the Waterways Experiment

Station in Vicksburg, Mississippi and the Coastal Engineering Research Center

in Washington, D. C.

Information on shoreline changes prior to the years of photographic record

were obtained from NOS hydrographic survey sheets dating to 1859 and high water

shoreline change maps prepared by the U.S. Army Coastal Engineering Research Cen-

ter, Washington, D.C. Shoreline positions along each survey line were input

to the IBM 370 to be included with the existing photographic information. This

work was done as two separate studies', one of Charleston County and the other

for Horry, Georgetown and Beau'fort Counties (see refs. 20 , 36 and 37).

Data Presentation

As previously discussed, an examination of short-term variability along

the coast can provide for a rapid estimate of shoreline behavior at any loca-

tion. However, this type of information might be misleading in certain instances.

Rapid changes which average out over a longer period of time can result in a

stable trend. A large amount of erosion observed as a short-term variation

could subsequently be balanced by a gain of sediment along the beach. For

that reason, another level of information, individual erosion-deposition graphs

have been included. In areas where changes are somewhat similar for large

stretches of coastline, only representative curves are shown on the figures.

In areas that exhibit higher coastline variability (especially near tidal in-

lets), all the data are presented. Erosion-deposition figures for all measured

stations have been prepared and can.be acquired from the Coastal Research Di-

vision, Department of Geology, University of South Carolina, Columbia, S. C.

The graphs that appear in this report (Figs. 45-61) are included only to il-

lustrate concepts and to provide a means for rapidly determining general trends

along various areas of the coast.

Figure 45. Erosion-deposition graphs for stations L-1 (Little River) to N-4 (Myrtle Beach).
These graphs show the individual changes that were measured from successive aerial photo-
graphs and coastal charts. A positively sloping line indicates net accretion; a negatively
sloping line shows net erosion. An adequate understanding of the variability along this
section of coastline can be achieved only through careful inspection of these individual
graphs. For example, the relatively high short-term variability seen at stations C-2 and
N-3 is the result of erosion occurring between 1940 and 1948 and 1952 and 1958. The high
variability seen at Little River Inlet (stations L-1 through L-5) on the other hand, is
Ln
J the result of repeated large-scale changes in shoreline position. This is related to the
constant shifting of the inlet and the resulting modifications in wave processes and sedi-
ment transport patterns along adjacent beaches. The variability seen at stations L-6 and
L-7 attest to the effect that even small inlets (Hog Inlet) can have on adjacent beaches.

0 4 KM
N,

+200
+2ooL-6
@+Ioo
YEARS
YEARS r, 1925 34 so 63
0 1873 192534 48 71 v0
z
N.1 z <
-100
00
+200 L-10
-200
-2ooL
1 +100 YEARS
01873 1925 42 12 73
Oxtv, z +200 L-7
�r
, WK V-3 -1 00 1+100 YEARS
-200 01173 [email protected] 18, 73
z +20or- L-3
200 - C-A illoo
4
1.100- YEARS 200 @z 1876 19253A 50 6373
0 1873 19AOAB_63 YEARS
zz:[email protected]@ +200 L-11 00-
z
<00 -2ooL
+100 YEARS +200 L-8
200- 01873 1925 A2 52 63
z 1+100 YEARS
1873 1925 34 A8 58, 73 -200 L-4
100
+200 N-2 z
-200 <
@+Ioo
@'+Ioa YEARS 1: 100
0 19AO 52 @61 73 u Z- @.73 192534 A.18 73
z 200 100 YEARS
-loc 200
-200L
@200- N-4 +200 - C-2 +200 L-9 +200 L-5
100 - YEARS i+100 YEARS 1+100
1873
1878 1940 52 63 73 01878 1940 52 6 .3 0 @@'34 A858 73
z 192534 AB 58 73 z
< YEARS .-100-
z z < YEARS
A < -1 00-
-1
00- L
. ....... -200 - -200
-200 -

Figure 46. Erosion-deposition curves for stations M-1 (Myrtle Beach) to G-4 (Garden City Beach).
The most noticeable characteristic of these curves is the nearly linear change at each station.
Un Stations M-4 and M-6 show steady, gradual erosion throughout the entire period of record. Changes
at stations M-2, G-1 and G-3 are consistently small. Intermediate stations behave similarly.

+200 m-2

+too YEARS
1878 19AO [email protected]
M-1 z
x-too-

200-

-+200-
!+too- YEARS
1878 1940 52163 [email protected]
0

-100

-200-

+200 1 M-6
i_+loo- rffA2S
5 0 Isis 119AO 52 373
z
0
20:

+20 G-1 +200 G-3
@+Ioo YEARS Z+100 YEARS
3 0.1972 1925 64!5058 73
50 63
z
872 1925 c
X -JOC'.
00
-200 200-

0 4 Km

Figure 47. Erosion-deposition curves for stations G-5 (Garden City Beach) to P-5 (near Pa wley's
Inlet). The curves show drastic changes in shoreline position in the vicinity of Murrells In-
let. The amount:,of erosion observed at stations south of Murrells Inlet is nearly equal to the
deposition portion of those curves from stations north of the inlet, indicating a shift of sedi-
ment rather than a total loss of sand from the system. These trends in the vicinity of Murrells
Inlet imply that the effect of migrating tidal inlets is much more important as a short-term
CS event. This is certainly an encouraging thought to those trying to relate tidal inlet processes
to changes on adjacent beaches.

Station X-1 and X-3 show only slight change over the short term. This is due to the.fact that
these figures are based only on erosion measured during the most recent 25 years of record.
This example illustrates, how, when using this type of information, the reader must consider
all the input he has into the problPm, including the erosion-deposition curves and common
sense. Th,[email protected] location of these stations on a spit flanking an extremely active inlet should in-
dicate to the prospective planner that these areas could be subject to sudden and extreme erosion.

+200- G-5 +200 X-1
!+too- YEARS !+too
1 1872 1925 405050 7 0 1172
0
z 192.5 A2 52 63
'45 < YEARS
x oo- -, 00
x
u
_200. 200 - - ----

+200 X-2 +200 - X-3
6 !*too i*100 - YEARS
5 '.7' 01872 1925 42 @51
z 0 1115 Al
00
M-100
X. I
200- -200-

3
[email protected] - Y_ 1. +20o Y-3 i.20OF Y-5
!,+100. !+too
2 -+1 00.
11 0 0 0 1872 YEARS
z 872 19 5 4 64 z 872
4 1925 z
X -100 YEA < 2 64 4 5 42 57 73
C 3 YE S T
x-100 101,
_200- 2
00 200-

+200- P-1
-20OF
P-2 +200- P.3
_i+Too -
YEARS !+too-
1872 1925 42 57 73 YEARS
0 1072 1925 42 @57. 73
z 0- 0
11872 1 12 17 13 5
-1 [email protected] YEARS -C
z
z 00 100 too
200 2001- V_ 200-
7
2 N
_*200- P-4 +200 P-5
A +100 - i+loo
0 1872 19? 574 0
z 1872 19",__
3 S7 73 z
< YEARS 25 42 57 73
-too- A
T too YEARS
-200.
4 4 KM -200

Figure 48. Erosion-deposition curves-for stations,D-1 (Debidue Island) to W-6 -(Santee
Islands). Note the rapid shoreline changes occurring in the vicinity of North Inlet
(stations D-3 to 1-3). The 3000 feet of shoreline advance at station D-5 between 1934
and 1942 is a result of the southward migration of the Debidue recurved spit past that
location and does not represent 3000 feet of steady shoreline advance along that trans-
sect. Note also the rapid and steady shoreline retreat shown at station 1-4. This ero-
sion is related to the occurrence of washover fans in the area.

ON Graphs W-1 through W-6 show shoreline retreat between 1952 and 1973. Inspection of
earlier coastal charts showed a different trend. The spit extending northward into
Winyah Bay was formed between 1908 and 1928. March deposition occurred subsequent to
spit development. Recent erosion is most likely related to damming of the Santee in
1939.

200 ' D-1 -.200' D-3
i,100- 1.100.
1872 1925 42
0 00
z 57 73 Z1872 1915 42
c YEARS '0 YEARS
X-100- m-100

-200 200

.200-

+too-
0 N. D.
z
l9A9f53 73
Y ARS
to()
x

-200

/3
+200r D-5 200 1.3
i+loo !.too.
o WD9 Z
@l .7 -2 0 19A9 53 73
1925 A2 57 73 z
4 -1 00 YtAR5 X - 100 - YEARS
-200 -200-

-200- I-A +200 1.6
i'+ 100 - FE+Ioo
0 1875 IR7i
z 0
192
0\5iS 49 63 73 Z 19 23 3 5 49 53 73
x 0 YEARS A YEARS
u0
X-lo
?00 -200

+200' S-1- +200- S-2
+too - + I oo - YEARS
D 19 4g 1875 1925 35 57 73
-N 0
z
K YEARS
-1 00 - x-100
u
-200- -200-

W-2 W-A
i+10 1952 i.100 1952
0 @17. 73 YEARS YEARS
0 13 z0
z
.4 00
u
200-

W-6
1-10 1952
[email protected]
13
YEARS
z
x
4 100

4 KM

Figure 49. Erosion-deposition graphs for Cape Romain and Raccoon Key. Graph
numbers refer to the reference points illustrated on the map above the graphs., I.J
Erosional areas are shaded. Cape Romain has undergone steady erosion during
the interval of study. However, at location 5, over 2QOO feet of accretion have
occurred since 1941 and 450 feet (135 m) of accretion,have occurred at location
1. The remainder of the reference localities are erosional. The recurved spit
at location 13 was not present during the interval 1941-1963. This spit, which
is over 4000 feet (120 m) long, accumulated between 1941 and 1968 and grew at
an average rate of about 145 feet (45 m) per year.

RACOON KEY CAPE R'OMAIN
5

0- cv) N cn m
V Ln Ln %0 N 2
ol ol [email protected] ol 0
0-

0 2500
-200- ......

c) N
................
cl) cn
+200

. .........
ol ol
0. 0.
...........
...... ol cn N cl) cl) ol cl) N cl) cl) 0-
10 V LO to .0
010, ol ol ol ol 0. ol ol ol
0 -
..... . . ........
...... ......
. . . . . . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . .. . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . . .
. . . ..... . . .
ON . . . . . .
. . . .. . . . . . . . . .
. . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . ... . . .. . . . . .
. . . . . . . . . . . . . . .
200- . . . . . .. . . . . . . . . . . . . 6

. . . . . . . . . . . . . . . . . . .
. . . . . . . . . . .

. . . . . . . . . .

. . . . . . . . . . .

. . . . ...... . . . . .

777r7777771
0

............. ... ....... ..............
............ ............. .........
....... ....... ...... ...... ........... .
........ ....

.... ...........
-200- ......- .......
..................................
....................... ..... -L . '.-- ..... .......
...........................
............I......
.... .... ........... .........
............ ............
........ ....
.........................
..... ..............................
. . . . . . . . . . .
. . . . . . . . . . . . ..... . . . . . . . . . . . .
. . . . . . . . . . . . .. . . . . . . . . . . . . . . .
. . . . . . . . . . . .

. . . . . . . . . . . . .......
. . . . . . . . . . . .
. . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . .. . . . . . . .. . . . . . .. . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . .
. . . . . . . . . .. . . . . . .
1 0
. . . . . . . . . .
. . . . . . . . . . .
. . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . .
. .. . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . .
: : ::::X
. . . . . . . . . . . . . . . ... . . . . . . . . . . . . . .
. . .. . . . . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . .
0 . . . . . . . . . . . . . . . ............... .
I I @. .. . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . . . . .
. . . . . . . . . .
. . . . . . . . . . . . . . . . . . . . .......
. . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . .
. . . . . . . . . . . . . . . . . . . .

Figure 50. Erosion-deposition graphs for Bull Island. Graph numbers
refer to the reference points illustrated on the map above the graphs.
Erosional areas are shaded. Note the extensive erosion at the north
end of Bull Island, which is open from all sides to wave attack. Over
350 feet (105 m) of long-term erosion is illustrated in graphs 1-4. The
south-central portion of the island is characterized by alternate ero-
sion and deposition (graphs 5-9). As much as 1000 feet of deposition
occurred between 1958 and 1963 at location 8.

BULL ISLAND

0 2500

m
9b 2
[email protected]@6 @5 +200- c.) N c.) co c-)
8 V to Lo 'o 'o
o. C),
0-
.................
...............
.............
......... .
.. ..........
............
-200-1

+200-
0
00 5 r.. 1:::::,l
o. A
V LO W) 'o
-200- [email protected] [email protected]

+200- cn
0- cn N cn N
V Lo in 0 C>@

..........
'[email protected] . ... . .. ...........
8 0 -T 1 1

... .......
. ........... ......
TT .. ........
-200-
0 0
0 0 0
+200

9 o I --r-T 7 r
...........
-200T
/scl,

Figure 51. Erosion-deposition curves for Capers Island. Note that all station .s
come within the effect of adjacent inlets and exhibit an unstable or erosional
character. The central and southwestern beaches have been strongly erosional
since historical coverage. In-place palmettoes can be seen on the present beach-
face. The accretion which occurred at station 6 was due to spit growth between
1921 and 1953 which narrowed Capers Inlet by 1000 feet. Graph 1 is measured
northeast into the inlet and exhibits erosion and deposition associated with slight
oscihations of the inlet channel. The erosional trends of the seaward side of
the island are clearly shown by graphs 2-5, which show beach erosion ranging from
between 300 and 1000 feet over the study period and acceleration of erosion with
time as indicated by a steepening of the downcurve. Graph 5 measures the accre-
tion of a spit system which is building into Capers Inlet to the southwest. The
trend for graph 6 indicates a southward migration of Capers Inlet between 1949 and
1958, then a gradual retreat to the north over the past fifteen years.

CAPERS ISLAND

0 1500

60 0 0 0
5 4 3

+200-
V C%4 cl) cl) cl) v C14 m cl) cl) 14 clq M cl) ce)
cn v W) 10 N C-) 't W) ON
ol ol Ol CN mv LO ON
ol 010, 0, 0, o'. 0, 0, 0, 0, 0, o- 0- [email protected] [email protected]

..............
........................
o .......... ........... ......
...........
....... . .......... ..............................
..........
......... ... . . ................... ..............................
............ .............. ............. ...... .................. .... ...... . ................
...........
.......... .............. ......- ........
. . ..............

.................................
.................. .
..........
.............
................ ......... -.......%....... .........
.................. ........ -.. ............ .......
................................
.................. 1-1- .... ..
..............
........... .......
. .......... ...... ... ........... .......
......................I...... ...... .... ......
......................
-20 ............ 1 [email protected]@
0- ......
.......... .... ......... ................
........... ............... ... ...
............
................... ..........
...........-...... .......
.................... ...
...............................
...... ..... ..........
..................
.... .... ..
................................
+200-
. .........
................
. ........... .. .. .... .............
......... .... ............

....... .......
...............
...............
0- ...... ........
..........

........... .........-

.. ........
-2001
............
...... ............

..............

........ ....

Figure 52. Erosion-deposition curves for Dewees Island. The northeastern
portion of the island (stations 0-2) has been characterized first by ac-
cretion since 1921. In contrast, the southwestern half of the island
(graphs 3-5) has experienced continuous erosion up to 2000 feet since 1972.
The accretion at stations 0 and 1 is related to the progradation of the
large spit subsequent to the shifting of Capers Inlet.

Ln 3

Cl 0

Lne

............

...........
We
19 21
3

1942
...... ..... . .
19 5 3
..................
1963
.............

............ .. ..... ...... ......
19 7 3"'

_I 2 6

...1886

..............

....1921

:1953
-1963
:'197 3

Figure 53. Erosion-deposition curves for the Isle of Palms. During t -he past
100 years, the northeastern end of the island (graphs 3-13) has been charac-
terized by periods of erosion followed by periods of accretion. This has
W been caused, in part, by changes of Dewees Inlet and its ebb-tidal delta.
The central and southwestern shorelines (graphs 15-25) have been accretional
or stable since 1872. A field of groins located along these beaches has been
partially responsible for this stability.

ISLE OF PALMS

0 1500
6==ffTTnmmli
m

25 23 21 19 17
+200- 15 13 11 9 %

3
0- J I I I I 1 1 12 15
-100
4200-
.9
/0-0
0- 1 r-T 23 11 1 1 1 1 T7 17

-100-
-#200-

25 3
'19 o, I
0- 111111
[email protected] m cn cn CN cn cn m CN cn M cn
-100- CN V Lo 10 N I q to 'o N v Lo @o N
0- ol 010, 0,- 0, 0,0, 0, 0.0%01

Figure 54. Erosion-deposition curves for Sullivans Island. Generally, the
island beaches have been relatively stable. The northeastern end of the
island (stations 2 and 4) has fluctuated in response to changes in the
Breaches Inlet ebb-tidal delta. The middle of the island (stations 6 and
8) was accretional between 1972 and 1921. Since that time, the shoreline
L.n has been variable. The beaches of the southwestern end of Sullivans Is-
land (graphs 10 and 12) have prograded more than 200 m since 197Z.

SULLIVANS ISLAND

2
0 1500
10 6 4

+200-

10 0- 1 1 111ir-1 6 1 1 1 1 T

-100-
+200-

12 o- 4
[email protected],Cvcn cn
[email protected] A C14 m Cl)
C'4 Cl) 11 to 10 N Cl) Iq LO 10 N C.) -.4 Lo 0N
-looj 0, 0, 0, ()@ 0, 0, [email protected] 01010, ol [email protected] 0, (>, C), C>. 0-

Figure 55. Erosion-deposition curves for Morris Island. The shoreline progradation
at station 1(1909-1939), 2 (1900-1953), 3 (1900-1939) and 4 (1900-1939) was due to
the recurved spit building into Charleston Harbor. The nearly constant shoreline
recession is probably a consequence of the Charleston Harbor jetty construction.
The project which was begun in the early 1860's and completed in 1896 caused less
sediment to be contributed to Morris Island and to the shoals which fronted the is-
land. Since emplacement of the jetties, these shoals have gradually disappeared,
and the resulting beach erosion has totalled 200-1250 m since 1864. The lack of a
well-developed foredune ridge on Morris Island has also contributed to the problem.

m =

ICo + 014
11 CA3 C.3
C) 0
0 00 00 0 0
3

...... ....
..........
......... .....
.......... .... ...........
...........

.. .......... 1900
....................
... ........ ...................
..... .. .......
................... ...... ......
.. ........................ 1909
..........
. ......... .....
...............................
..... ....
.............

.................................
.................................. ............
...................................
. ............. ..... .
A ...... . ....... 1934
...... .........
.......... 19 3 9
.. . ............
.. ..........
.............
....... ... ..........................
. .. .. .. ......... ..................... ....
...........
... ...... ........ 1949
. . ................
.......... ..... ..
.................... ................ ........ 11 ...
....... 1957
.............................
.................................. ...........................................
........................
...................... ...............
...........
..... .....
.. ............................ ....................
...........................
1968
.... ...................
................ ......
... ...... ...................
..... ......
........................ .......... ..................
00 1973

.... ... ....
...... ....

.............
... ......................

............ I...... ...
..................
...............
..........

. ... ........
.............. ...

..........
... ........
................. .... :::::::::
.................. ............. .....

..............
................
.........................

.............. ....... ..............
.......... .. ......
.........................
. ..... ....................... OAI ......

Figure 56. Erosion-deposition curves for Folly Island. Jetty construction at
Charleston Harbor between 1860-1869 and channel migration at Lighthouse Inlet
have affected shoreline changes at stations 2, 4, 5 and 8. Beach erosion was
continuous in the middle section of the island (graph 10 and 12) from 1857 to
1963, followed by a period of accretion and stabilization. The shoreline at
stations 14 and 16 have experienced serious erosion from 1857 to 1921. Since
that time, this section has been fairly stable. Shoreline stabilization at
Folly Island has been partially accomplished by the construction of breakwaters
and groins. Major shoreline changes can be expected after the next hurricane
and/or large storm. Because beach houses and other structures are so close to the
high water mark, the effect of a hurricane will be devastating.

FOLLY ISLAND

0 1500 *2 4300-
T!%iwiiii t
m
4 *2
8 6 .4
+200-
14

0 M 0, 0, MN cn 00 cn
ul 0 m m q V) W) 'o 'o N
co
0 4100-

o' m N m
q @nn 0,0 N

0 -
-100-
.......... ......
........................... ...
.....................
............................... .. .. .......... . .............. ... .
...........................
....... ..............
00
.... ............
. ..............

-100-
-200

.. ........
...........
..................
.................
.....................
14 o ..........
...........
.. ........ ....
..........

.......... ................ .......
..... ........ Z, ......
......................
-200-
......................... .....

-100-

+100- 06 0
98
-2001

.....................
... ............
16-500-

...... 100-

-600

Figure 57. Erosion-deposition graphs for Kiawah Island. Graph numbers refer
to the reference points illustrated on the map above the graphs. Erosional
areas are shaded. Note the large scale erosional (graphs 1 and 3) and depo-
00
sitional (graph 4) trends at the north end of Kiawah Island. These fluctua-
tions are related to changes in Stono Inlet. The midsection of Kiawah Island
is stable.

m MIMIM m m m m m M-MIM

+200- KIAWAH ISLAND [email protected] cn N cn cn
to LO 'o N
C->,
16 0--j
...... ...........
ol cn A [email protected]
v to LO %0 N
...............
.......................
Ol 0. ol ol 0. 5
7
N
-200 09 ........
...................
.......................
.................

.. ........ *........
..................

...................
...................
...................
................
.................
................
8

..........
0 5000
2
...........
..........
..........
..........
m
..........
18

+200-
8
0- (n cn
0 V Lo .0 N 0
ol ol [email protected] Ol ........... . . . .
3 ...........
. ..........
.... ........I

00
+200- 0. (1) Cl) m ................
......................................
V LO to 10 N
0,0,0, 0, ol
.....................................
T-1-1 T
................
20 0-
...........................
............................
...................................
...... ...................................
...............
10-
...........................
................ -- ........
.. .......................
...............................
...............................
................. I..............
...................................
.........................
............................ ......
.....................I.......
..................................
......................
-200- .........................................
--- ......................
..................................
..............

...........
5 r i I

................
.................. ......
12 ..........
..........
.................................... ..........
..................
21 y
................................. ..........
. ...........
200 ...... .

+200- 6
14
'2
8
[email protected]
4 09
0 ?6 0

22 o-'-.7.71,717

L -200-

Figure 58. Erosion-deposition graphs for Edingsville Beach. Graph numbers
indicate the reference points illustrated on the map above the graph.
Erosional areas are shaded. To avoid repetition, selected graphs are pre-
sented. This section of coastline has undergone continual erosion through-
out the entire study interval. Erosion-deposition graphs indicate 200 -
300 feet (60-90 m) at all localities except station G6. Between 1949 and
1954, the closing of a small inlet permitted accretion of over 200 feet at
00
station G6. Since that time, this area has eroded approximately 500 feet
(150 m).

EDINGSVILLE BEACH
-1!$Il 0 2500
1 [email protected] 1 1 @O9 @8 @76 @54 @32 @j m

0, C.) N cl) cl) cn ol cl) N cn M cn
14 to W) 10 N W) @o v Zn Lo o K v LO W) %0
D. 0. [email protected] ol ol 0, 0, 0, ol 0.01 ol ol ol ol [email protected] 0- ol
0
............
... .........
.... .......................
........ .......... .................
10 ........ ...................... ......... I....I........
.... ..... I. ..... .......................
. ..... .......
............
...................... .......................
................
00
.......................
..........
41 -200-
I ..........
....... ...............
...... .... .........
............ .....
............
.............
............
............

............
...........
............
............
............

...........
12 0 v I T "<<.I 8 6-4 1
. ..... .... ...........
. . ........
..............

.................
-200-
.............

.............
.............

.............

Figure 59. Erosion-deposition graphs for Edisto Island. Graph numbers
indicate the reference points illustrated on the map above the graph.
Erosional areas are shaded. Note the overall stability (graphs 5-11)
00
U1 of this island. The beach is dotted with a series of groins which help
stabilize the shoreline. Graphs 12 and 13 both indicate over 200 feet
(60 m) of erosion during the study interval. One hurricane, which oc-
curred in 1940, caused erosion ranging between 30 and 100 feet (10-30 m)
at Edisto Beach. However, recovery has occurred between the years of
0
photographic coverage so the presented graphs do not show this change.

EDISTO ISLAND 0 2500
62%-Mm
M Cl) 16 3 2 1 m
Lo to 10 N 15
0- 0. [email protected] 14 5
8 T cl) N cn Cl) cn N cv) Cl)
Lo Lo @o N
13 [email protected] C>. (>. ol [email protected] [email protected] o.
to to
12 ........
...... ....

-200J -j

+200-
tn tn cn @cn
@o h,
ol 0- 0- ol
cc 13 o-

-200J *@@i

+200- 10

15 o-

-200-J

+200-

16 o- -*T-TT-p
8

L----200-J
5 4 3
I
0 @6
c_) N
12 1

Figure 60. Erosion-deposition curves for stations H-1 (Hunting Island) to B-7 (Baypoint
Island). The overall trend in this area is one of continued and, in many cases, severe,
erosion. This is largely due to the effect of tidal inlets. The hardest hit areas
are stations H-1 through H-6 (Hunting Island) and A-1 through A-3 (Capers Island).
The retreat of Hunting Island is related to a reorientation of the beach in response
to waves traveling across open St. Helena Sound. We feel that the rapid erosion at
stations A-1, 2 and 3 is a function of coastal geomorphology. Unlike other barriers
in this area, there are no beach ridges on Capers Island. Elsewhere along the South
Carolina coast, areas lacking beach ridges have the highest erosion rates measured. This
area is characterized by severe washover and erosion rates in excess of 95 feet (29 m)
per year.

00 The only place not undergoing serious long-term erosion is the beach immediately to the
_J west of Fripp Inlet (stations F-1 through F-3). This is a natural process in which the
beach immediately downdrift of tidal inlets can build out due to the refraction of waves
around the ebb-tidal delta (outer bar). According to this concept, storm waves approach-
ing from the northeast would cause southward longshore sediment transport along Hunting
Island which is gradually realigning itself in response to these waves. Upon encountering
the shoals (ebb-tidal delta) of Fripp Inlet, however, the waves would be refracted (bent)
so that they would be approaching the beach from the south in the vicinity of stations
F-1, 2 and 3. This reversal in wave approach direction causes easterly transport at these
stations and the gradual building out of the beach in the area near the inlet. Despite
the long-term accretional tendency in this area, rapid erosion can occur (station F-1,
1955-60). Field studies have shown this area subject to frequent erosional episodes.

mid

0,
CHANGE IMI CHANGE IMI CHANGE ItAl CHANGE (Ml -
0 0 0 0 0
0 0 0 0 0 0 0 8 8 8
7

CHANGE(Ml CHANGE IMI

0
r
>

@MANGE IM) CHANGE IM) CHANGE (MI CHANGE (MI.. (a
0 0 0 0 0 .0 0

4A,

CHANGE[Ml CHANGE(MI CHANGE(Ml CHANGE [email protected] 11 In
0 o o o
0 0 0

CHANGE IM) HANGE (Ml CHANGE [m) CHANGE IM), @HANOE M
0
8 0 o o o

>
ol
W-0

Figure 61. Frosion-deposition curves for stations J-1 (Hilton Head Island to
Z-4 (Daufuskie Island). Despite the variability in shoreline change from
station to station, the overall trend in this area is one of stability.
00
When erosion occurs, it is generally slight. It appears that Hilton Head
is gradually becoming reoriented by erosion along its northern half (note
the truncated beach ridges at stations J-5, 6 and 7). Much of the sand
being added to the beach at stations T-1 through T-4 probably was derived
from this area. Daufuskie Island has undergone gradual retreat over the
period of record. In addition to wave action, tidal currents from Calibogue
Sound can be effective in removing sand from this beach.

2 Z-1
3 5
4 4
T-1

0 4 KM

+TOO- Z-4 +100 - U-6 +ioo U-2 +100 T-4 +100 - J-7
T y @E 1951
YEARS YEARS YEARS YEA
3
0 0 'S
0 19A2 55 66 19A2 55 66 73 0 /116 66 11
z z z z55 66 73 z
< < YEARS <

-100- -100 -100 - -100- -100-

+100- Z-2 +ioo - U-4 +100- T-6 +100- T-2

YEARS YEARS
o 1942 5.5 6-6 1942 55 66 73 00 1951 0 /15 66 73
z Z 0 z 5 z 0 1,951
< 66 73
YEARS
x
-100. -100 - 100 -100-

SUMMARY

Analyses of char t and aerial photographic data has been used to determine

short- and long-term beach erosion-deposition trends in South Carolina. These

data are a necessary consideration in the planning and development of the coast-

al zone, inasmuch as they can help to minimize economic losses resulting from

construction in unstable ar eas.

Users of this information are reminded that the relative stability of a

shoreline must be considered on two levels:

First: The long-term stability of a beach area is the rate

at which it is either prograding or retreating over a

period of, say, 50 or .100 years. It is reflected in

major reorganizations of the shoreline morphology and is

probably caused by changes in local wave climate or sedi-

ment supply. Considerations of these rates of change are

important but certainly not all-inclusive, because they

only indicate the net change in a shoreline position and

shed no light on shorter-term events.

Second: The short-term stability of a beach area is the extent to

which the shoreline fluctuates over periods of months or

years, usually in response to storm conditions. These fluc-

tuations are superimposed on the longer-term changes and are

probably the most important to consider in terms of where to

best locate a home or business.

Certain generalizations are possible regarding the overall trends of

erosion and deposition on the South Carolina coast:

The grand strand area is relatively stable. Exceptions occur

In the vicinity of Little River, Murrells and other small tidal

inlets. The extent of the inlet's influence is a function of

the size of the inlet and the distance over which it migrates.

Other portions of the coast exhibit varying degrees of

stability, depending upon inlet size and frequency. In

areas where moderate sized tidal inlets are separated by

more than 6-9.5 miles (10-15 km). the area midway between

the inlets generally exhibits the greatest stability.

Shoreline variations increase in either direction toward

the inlets. In areas where inlets are much closer to-

gether and much larger (Beaufort County), few sections of

beach are outside the effects of the neighboring tidal in-

lets. In these areas, a complex history results which is

closely tied to changes in the patterns of movement of the

nearby inlets.

ACKNOWLEDGEMENTS

This report was prepared for the South Carolina Coastal Council (Dr.

Wayne Beam, Director). Much of the original data upon which this report is

based was collected as part of two research projects sponsored by the South

Carolina Sea Grant Program (Contract nos. 04-6-158-44096 and 04-6-148-44096,

Miles 0. Hayes, Principal Investigator). Other data were collected while

under contract with the Coastal Engineering Research Center (Contract No.

DACW72-74-C-0018) and the Army Research Office (Contract No. DAAG-29-76-6-

0111). Other funds were provided by the Dept. of Geology, University of

South Carolina.

Many of the ideas and much of the field work and data analysis that con-

tributed to this project were provided by members of the Coastal Research Di-

vision, Dept. of Geology (U.S.C.), including: Dag Nummedal, Michael Stephen,

Duncan FitzGerald, Timothy Kana, Robert Finley, Carey Fico, P. Jeffrey Brown,

Stan Humphries, Jeff Knoth, and John Barwis. Timothy Kana is acknowledged for

his assistance in editing the manuscript. The authors would also like to thank

Pris Ridgell, Nannette Muzzy, Burk Scheper and Helen Mary Johnson for their

skilled technical assistance in preparation of this report.

GLOSSARY OF TERMS

Accretion - The build up of sand on a beach causing the shoreline to move
seaward. An advantageous situation if you are a,property owner at an
accreting beach site.

Barrier Island - A long, generally narrow, island separated from the main-
land by a lagoon, tidal creeks or marsh, which protects inland areas from
destructive ocean waves.

Bathymetry - The measurement of water depths and charting of the topography
of the sea floor.

Beach - A gently sloping zone of loose sand or shell material exposed to
waves along a shoreline.

Beachface - The portion of the beach ordinarily traversed by the uprush and
backrush of waves as the tide rises and falls.

Beach profile - A cut-away view of a section of beach drawn perpendicular
to the shoreline, which shows changes in topography.

Beach ridge - A long, low mount of sand located landward of the active beach,
which is no longer building up and may be heavily vegetated. It generally
marks the position of an ancient shoreline and often occur in sets of nearly
parallel ridges.

Berm - The zone of beach between the foredunes and the beachface, generally
flat and nearly horizontal. Indicative of an accretional beach. The wider
the berm, the more protection from storm waves. In general, berms are
severely eroded during storms but build up again between storms.

Breaker - A breaking wave along the shoreline. Types include spilling,
plunging, collapsing and surging.

Coastal plain - In. S. C., it is a broad geologic province of nearly flat,
low-lying sedimentary deposits between the Piedmont (e.g. near Columbia)
and the ocean coast.

Current - A flow of water generated by tides or waves which is important in
moving sand from one place to another.

Downdrift - Direction toward which a current is flowing. Opposite of updrift.
In reference to a jetty or groin, the downdrift side is generally erosional
since sand cannot efficiently pass through the barrier but is trapped on the
updrift side.

Dunes - Wind blown deposits of sand common along the seaward margins of
barrier islands (see Foredune ridge).

Ebb-Tidal Delta - A delta-like deposit of sand just seaward of a tidal inlet
posing a hazard to navigation, but often protecting adjacent beaches from
severe erosion.

Erosion - Removal of sand from the shore by the action of waves during storms,
or by tidal currents in an inlet or tidal channel. Opposite of accretion.

Fetch - The area of sea surface over which the wind blows and generates waves.

Foredune Ridge - The seaward-most ridge of sand parallel to the shoreline which
protects inland areas from erosion by waves during storms. The higher the
ridge, the more protection to the coastal property.

Geomorphology - The study of landforms, their description, classification,
origin and development.

Groin - A man-made structure of rocks, pilings, etc., built into the ocean
from the beach, intended to trap sand moving alongshore. Tends to accumu-
late sand on its updrift side, but often accelerates erosion on the down-
drift side.

Hurricane - A tropical storm of severe intensity, originating in the Carib-
bean with counterclockwise winds greater than 75 mph, revolving around a
low pressure center (eye).

Inlet - A short, narrow waterway connecting the sea with an inland waterbody.

Intertidal Zone - The area along the shore which is alternately covered at
high water and exposed at low water.

Jetty - A structure extending out from the shore into a body ofwater designed
to direct and confine the current or tide. Commonly intended to protect a
harbor, prevent shoaling of navigable waterways, etc.

Littoral Zone - The zone along the shore affected by waves and tides.

Longshore Current - (littoral current) The nearshore current, generated by
waves breaking obliquely with the shoreline, running parallel to the shore.

Longshore Drift - The sedimentary material moved alongshore under the influence
of waves and currents.

Longshore Transport - The active transport of sedimentary material parallel
to shore. A typical rate for South Carolina is.100-200,000 cubic yards
per year.

Outcrop - The portion of a geologic structure or layer which is exposed at
the surface.

Prograde - To build out, as in: A beach which is accreting, progrades toward
the sea.

Recurved Spit Most common at the southern end of South Carolina barrier is-
lands formed by sand transported alongshore and deposited in a curving spit-
like ridge near an inlet. Examples - Debidue Island, Bull Island, Isle of
Palms, Kiawah Island, etc.

Ridge and Runnel - A long, linear, intertidal bar of sand (ridge) separated
from the beachface by a shallow trough (runnel) which tends to migrate up
the beach during moderate wave conditions adding new sediment to the shoreline.

Storm Surge - The additional water level added to normal tides caused by winds
piling waters against the coast during storms. Allows waves to attack higher
elevations. Storm surges up to 10 feet above mean sea level have been re-
corded in South Carolina.

Surf Zone - The area between the outermost line of breakers and the limit of
wave uprush.

Swash Line - A line of debris left at the upper limit of wave uprush on a beach.
Important in marking the extent of wave attack during storms.

Swash Zone - The area of wave uprush and backrush along a beachface.

Tide - The normal rise and fall of water levels due to the rotation of the earth
around the sun and the moon around the earth. South Carolina has a semi-
diurnal (twice daily) tide with two high tides and two low tides occurring
each day. Tide range is approximately 6 feet.

Updrift - Direction from which a current is flowing. Opposite of downdrift.
The updrift side of a groin is generally a zone of accumulation of sand.

Washover - A flat, fan-shaped deposit of sand washed onshore during a storm,
which may cover inland marsh areas. Examples: Morris.Island, Edingsville
Beach.

LIST OF REFERENCES

1. Aburawi, R. M., 1972, Sedimentary facies of the Holocene Santee delta: un-
pub. M. S. thesis, University of South Carolina, Columbia, S. C., 96p.

2. Brown, P. J., 1977, Variations in South Carolina coastal morphology:
Southeastern Geology, v. 18, no. 4, p. 249-264.

3. Coastal Engineering Research Center, 1973, Shore Protection Manual, 3
vols.: U.S. Govt. Printing Office, Washington, D. C.

4. Crutcher, H. D., and Quayle, R. C., 1974, Mariners worldwide climate guide
to tropical storms at sea: Naval Weather Service Command, U. S. Dept.
of Commerce, Wash., D. C.

5. Dean, R. G. and Walton, T. L., 1975, Sediment transport processes in the
vicinity of inlets with special reference to sand trapping: in Cronin,
L, E., ed., Estuarine Research, Geology and Engineering: Academic Press,
N. Y., v. 2, p. 129-150.

6. Dunn, G. E., and Miller, E. 1., 1960, Atlantic hurricanes: Louisiana State
University Press, Baton Rouge, La., 326p.

7. Emery, K. 0., 1961, A simple method of measuring beach profiles: Limnology
and Oceanography, v. 6, p. 90-93.

8. Fico, C., 1977, Wave refraction studies on the South Carolina coast: in
Nummedal, D., ed., Beaches and Barriers of the Central South Car-olina
Coast, Guidebook for Fieldtrip "Coastal Sediments '77", 73p.

9. Finley, R. J., 1976, Hydraulics and dynamics of North Inlet 1974/1975:
GITI Report 10, U. S. Army, Corps of Engineers.

10. Hayes, M. 0., 1967, Hurricanes as geological agents: case studies of hur-
ricanes Carla, 1961, and Cindy, 1963: Rept. Invest. 61, Bur. Econ.
Geology, Univ. of Texas, Austin, Texas, 54p.

11. Owens, E. H., Hubbard, d. K., and Abele, R. W., 1973, The inves-
tigation of form and processes in the coastal zone: in Coates, D. R.,
ed., Coastal Geomorphology, Publications in [email protected], Bingham-
ton, N. Y., p. 11-41.

12. , Hulmes, L. J., and Wilson, S. J., 1974, Importance of tidal deltas
in erosional and depositional history of barrier islands: (abs.): in
Abstracts with Programs, 1974 Annual Meeting, Geol. Soc. of Am.,
Miami, Fla.

13. FitzGerald, D. M., Hulmes, L. J., and Wilson, S. J., 1976, Geomor-
phology of Kiawah Island, South Carolina: in Hayes, M. 0. and Kana,
T. W., eds., Terrigenous Clastic Depositional Environments: Tech.
Rept. No. 11-CRD, University of South Carolina, p. 11-80 - II-100.

14. and Kana, T. W., 1976, eds., Terrigenous Clastic Depositional En-
vironments: Tech. Rept. No. ll-CRD, University of South Carolina.

15. 1977, Development of Kiawah Island, South Carolina: Proceedings,
Conf. on Coastal Sediments '77, ASCE, Charleston, S. C., p. 828-847.

16. Hicks, S. D., 1972, On the classi fication and trends of long period sea
level rise: Shore and Beach, v. 40, p. 20-23.

17. and Crosby, James E., 1974, Trend and variability of yearly
mean sea level 1893-1972: NOAA Technical Memorandum NOS-13, National
Ocean Survey, National Oceanic and Atmospheric Admin., U. S. Dept.
of Commerce, Rockville, Md., 14p.

18. Hosier, P. E., 1975, Dunes and marsh vegetation: in Environmental Inven-
tory of Kiawah Island, ERC, Columbia, S. C., p. D-1 - D-94.

19. Hubbard, D. K. and Barwis, J. H., 1976, Discussion of tidal inlet sand
deposits: examples from the South Carolina coast: in Hayes, M. 0.
and Kana, T. W., eds., Terrigenous Clastic Depositional Environments,
Tech. Rept. No. 11-CRD, Univ. of South Carolina, p. 11-128 - 11-142.

20. , Lesesne, F., Stephen, M. F. and Hayes,
M. 0., 1977, Beach erosion inventory'of Horry, Georgetown and Beau-
fort Counties, South Carolina: S. C. Sea Grant Tech. Rept. No. 8, 58p.

21. Johnson, H.S. Jr. and DuBar, J. R., 1964, Geomorphic elements of the area
between the Cape Fear and Pee Dee Rivers, North and South Carolina:
Southeastern Geology, v. 5, no. 1, p. 37-48.

22. Kana, T. W., 1977a, Beach erosion during minor storm: Journal of the Water-
way, Port, Coastal and Ocean Division, ASCE, vol. 103, no. WW4, Proc.
Paper 13335, Nov. 1977, p. 505-518.

23. , 1977b, Suspended sediment transport at Price Inlet, S. C.:
Proceedings, Conf. on Coastal Sediments '77, ASCE, Charleston, S. C.,
p. 366-382.

24. and Knoth, J. S., 1977, Longshore sediment transport rates in
South Carolina: in Nummedal, Dag, ed., Beaches and Barriers of the
Central South Ca:-rolina Coast, "Coa-stal Sediments '77", Fieldtrip
Guidebook, p. 39-44.

25. Kraft, John C., 1971, Sedimentary facies patterns and geologic history of
a Holocene marine transgression: Geol. Soc. Amer. Bull., v. 82, p. 2131-
2158.

26. Landers, H., 1970, Climate of South Carolina: in Climates of the states:
South Carolina: Climatography.of the [email protected]_d States, No. 6038, ESSA
Environmental Data Service.

21, Millas, Jose Carlos, 1118, Hurricanes of the Caribbean and adjacent regions:
1492-1800: Academy of Arts and Sciences of the Americas, Miami, Fla.,
328p.

28. Milliman, J. D. and Emery, K. 0., 1968, Sea levels during the past 35,000
years: Science, v. 162, p. 1121-1123.

29, Myers, V. A*, 1915, Storm tide frequencies on the South Carolina coast:
NOAA Tech. Rept. NWS-16, 79p.

30. Nummedal, D. and Humphries, S. M., (in press), Hydraulics and dynamics of
North Inlet, S. C. 1975/76: U.S. Army Corps of Engineers.

31. Pilkey, 0. H., Jr., Pilkey, O.H., Sr. and Turner, R., 1975, How to live
with an island: Raleigh, North Carolina Dept. Nat. and Economic
Resources, 119p.

32. Pore, N.A., 1961, The storm surge: Mariners Weather Log, v. 5, no. 5, p.
151-156.

33. Price, W. Armstrong, 1955, Correlation of shoreline type with offshore
bottom conditions: Dept. of Oceanography, A&M College of Texas, Pro-
ject 53.

34. Shepard, F. P. and Wanless, H. R., 1971, Our changing coastlines: McGraw-
Hill, New York, N. Y., 579p.

35. South Carolina Parks, Recreation and Tourism Commission, 1976: South Caro-
lina'a beaches, 10p.

36. Stafford,.D. B., 1971, An aerial photographic technique for beach erosion
surveys in North Carolina, TM-36, U.S. Army, Corps of Engineers,
Coastal Eng. Res. Center, Wash., D. C.

37. Stephen, M. F., Brown, P. J., FitzGerald, D. M., Hubbard, D. K., and Hayes,
M. 0., 1975, Beach erosion inventory of Charleston County, South Caro-
lina: a preliminary report: S. C. Sea Grant Tech. Rept. No. 4., 79p

38. U.S. Army Corps of Engineers, 1957, U.S. Army Engineer District, Charles-
ton, S. C., Appraisal report - Investigation on hurricanes and asso-
ciated problems along the South Carolina Coast, 37p.

39. , 1971, National shoreline study, Great Lakes
Region - Inventory Report.

40. U.S. Naval Weather Service Command, 1970, Su-,mnary of Synoptic Meteorologi-
cal Observations, North American Coastal Marine Areas: National Climate
Center, Asheville, N. C., vol. 3.

NUNN
3 668 00001 5195