Physical Geology lecture outline - Coastal Processes

Lecture index:


What shapes coastlines?

Coastlines are the interface between the terrestrial and the marine and as such very dynamic locations.

What are the processes that move sediment, shape coastal landforms, and determine the geologic evolution of coastlines?

waves:

storms:

tides.

river sedimentation ('deltaic' forces): supplier of sediment.

biologic processes(esp. reefs, mangrove swamps).

Other factors/processes:

The result of this complex interplay is a great diversity of coastlines. We will look at just three types:

Deltaic complexes


Image of a delta building out into a fjord in Svalbard. Since this fjord was occupied by ice some 15,000 years ago or less, we know this delta has built out in that time period. Note the active portion to the left where transport and deposition is occurring via a braided stream. The oldest portion of the delta surface is the darker surface, where tundra vegetation has had a chance to establish itself. The braided stream has wandered back and forth over the delta surface with time. Note also the thin narrow beach ridge that has trapped small ponds behind it. What process is it that forms the smooth beach ridge, and why doesn't the delta have a birds-foot shape? Remember that this is in a more sheltered fjord.


Definition of a delta: body of sediment that forms and builds out where a river meets a lake or the sea.

How can deltas be classified?

Subsidence and mass wasting as contributing processes.

Evolution of in map view, lobe switching and abandonment.

This diagram is a repeat of material already presented (the portion on shifting depositional environments), and captures how with progradation the geologic record a delta is expected to produce is a grain size coarsening upward sequence.


Barrier Island complexes

Barrier islands are relatively long and sandy islands parallel to the coast, with lagoons or bays behind them. They are common with low profile sandy slopes, e.g. associated with coastal plains. The island is fundamentally caused by wave action piling up sediment and vegetation working to stabilize it.

Better known examples of barrier islands include: Padre Island, Galveston, Hilton Head - common along the Gulf Coast and southern half of east coast of the U.S..

Air photo mosaic images of barrier island complexes SE of Savannah Georgia taken from USGS ( now defunct terraserver site). In this particular case the barrier islands appear attached to the mainland by tidal flat areas, but are separated from the mainland by tidal channels.

This is a photo mosaic form USGS (terraserver site) of Gulf coast barrier island SW of Houston with some of the major island components labeled.

This is a false color satellite image of thin barrier island complexes along North Carolina coast that includes Kitty Hawk.

Geomorphic components of the system include: offshore sand bars, shore face, dunes, spillover fans, tidal channels, lagoonal area. You will work with these more in an upcoming lab

Diagram from USGS site http://3dparks.wr.usgs.gov/nyc/shoreline/beaches.htm that shows many of the components of a barrier island, with older, now submerged deposits when sea level was at a lower level.

Character of sediments in different portions of the complex?

Dynamics of change?

storms:

What will cause barrier island dynamics to change and migrations of the islands to occur?

Simplified navigation map of Tybee Island area near Savannah, Georgia

This is a dead oyster bed on the ocean shore face of Little Tybee Island which tells a story. Oysters like to grow in the protected tidal areas in back of the barrier islands, and not out in the shore face or open ocean environment. The oysters are bleached and no longer living, and one can also see the remnants of tidal marsh grass and organic rich sediments they once grew on here. There used to part of Tybee island in between this location and the ocean, but it has since retreated toward the land, over this once protected, tidal marsh area, leaving it exposed to ocean waves and erosion.

This is also on Tybee island and shows the beach sands advancing inland over the tidal marsh grasses. These photos were taken on a UNO geology field trip.

This is the shore face part of a barrier island on the Gulf side of Florida (near Balk Point State Park. Clearly the shore face is undergoing substantial erosion and retreat here.

Same barrier island as above, and view of a small curved sand spit on the end of the larger spit, with UNO students for scale. Barrier Islands can grow in length as new sand accumulates at spits end.

Spits end for now.


Emergent coastlines

Some features associated with emergent coastlines - sea cliffs, wave cut terraces, sea stacks, sea caves, sea arches. Differential erosion plays an important role in the production of the later three.

Importance of wave cut terrace formation: undercutting, mass wasting, and with time sea cliff retreat.

Examples: sections of California's coast line due to tectonics, and large parts of the Arctic due to rebound from glacial retreat and unloading.

Example from Festningen, Spitsbergen. This is a part of an Arctic archipelago that is undergoing isostatic uplift because of deglaciation. One can see the present shoreline with the retreating cliff line, and then a topographic bench in the image center - this is the old wave cut terrace where waves used to do their work, and the now weathered and subdued steeper slope to the right is an older and degraded sea cliff that marked an older and now uplifted shoreline.

Why are discrete 'steps' seen? One explanation can be a spurt of relatively sudden uplift. However, tectonic forces tend to be more steady. Another possibility is the interplay between sea level rise and tectonics. When sea level rise approximately matches tectonic uplift then the waves will cut at the same level for a longer time, and can form a notch, i.e. a wave cut platform.


This is a photo of some sea cliffs that surround Bear Island (Bjørnøya) on the Barents Shelf. The upper flat surface was due to erosion by an ice sheet. Since then waves have cut back into the bedrock to create these sea cliffs. The bays form along material that is easier to erode while the headlands are more resistant.

 


In this photo, also from Bear Island, the surface zone outlines a shallow and relatively flat area that is being cut by constant wave action - i.e. a wave cut terrace in the process of being formed. Note the sea cliffs in the back, with some talus at their base. Here the process of undercutting and mass wasting are important.

 


In this photo from Bear Island a sea arch has formed as the waves have cut through a rock fin of dipping strata with softer shales beneath harder sandstones. This is one of a number of erosional features such as sea stacks and sea caves, that form along erosional and emergent coastlines. The rebound of the crust after the glaciers melted away makes many coastlines in the Arctic area emergent.


This is a photo from a mountain top looking down on curved beach ridges in Svalbard. There are literally scores of beach ridges here, marking the gradual rise of the land out of the sea. Each beach ridge is made up of coarse gravel, and it is possible to fine driftwood and whalebones in some of them. The uplift is due to glacial rebound and associated unloading. An active surf zone can be seen on the far shore and the process continues, although probably at a decreasing rate.

 


This is a view offshore from Goat Rock along the northern California coast. A flat topped sea stack has a well developed sea arch that the waves have carved into it. Also, note the zone of surf - here the waves are in the process of carving a wave cut platform, which when elevated by tectonics can form a wave cut terrace. The flat top of the sea stack may be the remnants of such a terrace. Click on the image for a larger version.


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