Last week’s post showed some of the effects of erosion along the banks of the Potomac River, which flows lazily along a broad floodplain while not becoming so sluggish that it meanders. We know this condition doesn’t last, however, because the broad and anastomosed channels of the Potomac are forced into a narrow throat bordered by immovable Precambrian schist, as we discovered in a previous field trip. Today I am going to approach this series of cataracts from upstream and document the changing river morphology (Fig. 1).

Previous posts have described the floodplain morphology from Algonkian Regional Park (circled area to the upper left of Fig. 1) to the west (upstream), a terrain defined by relict riverbed topography incised by modern stream erosion from the surrounding terraces. At the other extreme, we visited Great Falls in a previous post, where we discovered Precambrian schists that resisted the river’s erosional power.

The field trip began at the Nature Center (black circle at top of Riverbend Park inset map). We followed a trail over poorly sorted gravelly sand (Fig. 2) cut by numerous channels, through what appeared to be a mature and healthy forest. I don’t know what kinds of trees they were but they were at least 80 feet in height.

The assortment of gravel and boulders seen in Fig. 2 is classified as a conglomerate. The rounded boulders and poor sorting suggests that these are fluvial. The boulders became round by rolling along the bottom of the river. This conglomerate (sediment is an unconsolidated rock to a geologist) is matrix supported, which suggests that high-flow events were common, but the majority of the sediment was the product of chemical weathering of rocks like the diabase we saw in a previous post. (Minerals with complex compositions react to water easily, compared to quartz.)

I will return to this later in the post.

However, there were angular pieces of a fissile, dark rock showing up as regolith along the trail (Fig. 3), suggesting that the conglomeratic sediments were a thin veneer over resistant bedrock.

The trail dropped to the river where outcrops of resistant bedrock appeared within the shallow river channel (Fig. 4). This was a substantial change from a few miles upstream

Our path follows the red line along the river bank in the Riverbend inset map of Fig. 2. We are approaching Great Falls. The trail is no longer constructed on conglomerate, but now is traversing sandy silt sediments deposited during the Holocene epoch (Fig. 5).

Schistose rocks with nearly vertical layering appear along the riverbank, and begin to obstruct the trail (Figs. 6 and 7).

Our short hike led to the Aqueduct damn, which supplies water to Washington DC (Fig. 9), where the river transforms into a raging torrent that is challenged only by experienced kayakers.

The transformation of the Potomac, from the placid stream in Fig. 4, to the convoluted and dangerous channel that follows no commonsense rules of river flow seen in Fig. 11, took place in less than two miles (see Fig. 1). I know because I walked the river bank, passing from one era to another before being confronted by a past that will not die…

There is one last point I’d like to make in this post. The imposition of Holocene erosion–streams fed by the Pleistocene highlands bounding the Potomac floodplain–applies here as well as in the gentler topography we saw upstream. The transition from the conglomerate we saw at a major stream draining into the Potomac (Fig. 2) to the more typical fluvial sediment (sand/silt/mud) we found further downstream (Fig. 5) reflects the input of erosion of bedrock only a few miles from the Potomac. This was documented in a previous post, which showed the breakdown of regolith into cobbles, which were transported inexorably to the Potomac.

It is my opinion that this is what has been recorded in the rocks along the banks of the Potomac River, creating the juxtaposition of sediment types along the path of a river that is draining the roots of an ancient mountain range.

This post returns to the Potomac River. We have previously discussed several features along this stretch of the famous waterway: Precambrian metamorphic rocks at Great Falls; sediment contributed by tributaries as well as erosion; and emplacement of intrusive rocks during rifting of Pangea to form the Atlantic Ocean. This time we’ll see evidence of recent erosion, as evidenced in Fig. 1, which shows a large block of stone that has collapsed along the steeply eroded south bank. The bank consists of silt and clay just like further upstream.

Site A (see Fig. 2) is where Fig. 1 was taken. The meandering stream to the east in Fig. 2 is Sugarland Run, which we examined further south, near its headwaters, in a previous post. The Rock-D geologic map suggests that the river is underlain by a Triassic (237-203 Ma) fining-upward sedimentary sequence consisting of sands to shales. A close-up image of the boulder at Site A (Fig. 3), despite a covering of mud and some biological material, reveals no apparent bedding. This is contrary to the description of the Balls Bluff (sedimentary) Member of the Bull Run Formation, contemporaneous with the Newark Supergroup although no longer considered stratigraphically equivalent.

Figure 3 doesn’t look sedimentary to me, but more like the diabase we saw further upstream on Sugarland Run. The streak of white material in the upper-left corner looks like quartz. If these are Triassic sedimentary rocks, they wouldn’t have been metamorphosed, so this exposed block is anomalous. It is possible that this is an outlier of sedimentary rocks that were thermally altered when intrusive rocks were emplaced during Triassic. The area consists of faulted and folded diabase, sedimentary rocks, and metasediments–intruded, deposited or altered, respectively, during the breakup of Pangea during the Triassic period.

The bank is steeply eroded with trees collapsing into the river, indicating rapid lateral erosion during the lifetime of a typical tree (less than a century).

This section of the southern flank of the Potomac River is characterized by a wide floodplain covered with hummocks that represent bars on the original river bed. Superimposed on this older morphology is a natural levee (Fig. 7) that varies in height, steepness, and distance from the modern channel along the river. This landscape has been cut by numerous streams that drain the Pleistocene highlands overlooking the incised river.

Substantial islands (Figs. 5 and 6)divide the Potomac river into two anastomosed channels (see Fig. 2) that have become unstable during the last ten thousand years, as demonstrated by rapid downcutting and lateral instability (Figs. 1 and 4).