St. Francois Mountains Trip - Missouri

As one of the duties of a geology lab instructor, last spring I went on a trip to the St. Francois Mountains in southeast Missouri. These are a range of Precambrian igneous rocks which stand in slight contrast the surrounding sedimentary rocks.

These igneous rocks formed around 1.5 billion years ago. In contrast, the surrounding sedimentary rocks are Cambrian in age, around 500 million years old. This results in a large buttress unconformity between the older igneous and younger sedimentary rocks. Both intrusive and extrusive igneous rocks are found throughout the "mountains", which is the remnant of largescale volcanic and intrusive activity.

Stop 1: Johnson's Shut-Ins State park.

The first stop of the trip was to Johnson's Shut-Ins State Park. This is a popular visitor site in the area, but was closed between 2005 and 2009 due to the Tom Sauk reservoir breaking and flooding the park. The evidence of this flood is still seen near the visitor center in the form of a land scar, with missing trees and large boulders strewn about the field.

The scar from the flood due the failing of the hilltop reservoir. The boulders in the field were carried by the floodwaters.

Part of the lawsuit winnings against the company that owned the reservoir have gone to current and future part improvements. One of the interesting details of the visitor center was the types of rocks used in the construction, which represent the local geology.

Rock types used for the Johnson's Shut-Ins State Park Visitor Center. The purple rocks are the local rhyolite, while the overlying rocks are sedimentary. This shows the contrast between the igneous rocks and the flat-lying sedimentary rocks.

Many of the ground tiles around the park are inlaid with interesting rock types. Although these are not local rock types, they are still fun to look at.

There was only one improvement which bothered me...

Rhylite..?

From the visitor center we walked up to the actual Shut-Ins. Along the way, we were reminded of the dangers posed by the reservoir.



200 steps. No more, no less.

The Shut-Ins are a result of the East Fork Black River eroding down through the originally overlying sedimentary layers (which are easily eroded) and eventually hitting the igneous rock below, which is more resistant to erosion. Due to this resistance, a "shut-ins" occurs, or a section of stream which is channeled through a narrow gorge.

Topographic map of Johnson Shut-Ins State Park. The East Fork Black River is shut-in, forming a narrow canyon, due to contact with the more resistant igneous rocks. The reservoir is also shown.

East Fork Black River, upstream from the Shut-Ins

East Fork Black River, downstream is the Shut-Ins, where the stream gets bottle-necked

Rhyolite porphyry make up Johnson's Shut-Ins. This rock type forms during volcanic eruptions.

The rocks of Johnson's Shut-Ins are heavily fractured. These fractures are nearly vertical.

Water erodes along zones of weakness. For this rock, it is the vertical fractures. The Shut-Ins contains many small falls and riffle pools.

Geology students: time to leave the path

Vertical fractures in the Shut-Ins rock often come in orthogonal pairs

In places the rhyolite contained these large white clasts (about 2 inches across at most) which were often eroded out as hollows. These white clasts are pumice inclusions in the rhyolite, mixed in during volcanic eruptions

Crossing the Shut-Ins, we encountered this cross-bedding in the sedimentary rocks above the rhyolite.

Stop 2: Elephant Rocks State Park

The next stop was to visit Elephant Rocks State Park. This park consists of a dome of granite which is heavily fractured. This fracturing is a result of pressure being released from the granitic rocks, which originally cooled deep underground and under high pressures but which are now exposed at the surface. This type of mechanical unloading creates both vertical and horizontal fractures in the rock, perfect for quarrying. This goes to show how much overlying rock has been removed since then. Erosion around the fractures produces large, rounded boulders which supposedly resemble elephants.

The rocks formed here are compositionally similar to the rhyolite from Johnson's Shut-Ins, but formed deep underground, as opposed to explosive volcanic processes. This results in a coarser-grained igneous rock, as longer cooling times result in larger crystals.

Granite of the St. Francois Mountains, mostly consisting of potassium feldspar (pink crystals) and quartz (gray/white crystals)

Sitting atop the elephant rocks. The horizontal fracture is due to exfoliation of the granite from pressure unloading.



Looking down from the top of Elephant Rocks State Park. The rounded boulders of pink granite were likened to elephants.

Strolling atop the pink granite.

Large remnant granite boulder (the biggest elephant). Great for climbing on or crawling under and pretending to hold up in hilarious photographs

Quarry pond down down one of the trails at the park.

Stop 3: Ignimbrite Flows

The next stop was to see some ignimbrite, a fine-grained extrusive rock similar to rhyolite. These included very large, very thick exposures of volcanic rock which were the result of very large and very explosive eruptions. Since this was our first stop which wasn't a public park, it was also the first time students got to use a rock hammer (finally, the chance to hit rocks with hammers!).

A single layer of ignimbrite, deposited during a single eruption event.

Hand sample of the ignimbrite.

Important lessons on the correct way to break a rock and not the hammer

Intro geology students hitting rocks with hammers...I'll keep my distance

Stop 4: Mafic dike and the 1 billion year gap

The next stop was a combined geologic spectacle: a mafic dike through the felsic igneous rocks, and the gap in rock between the igneous rocks and the overlying sedimentary rocks.

A mafic dike can be seen sticking almost vertically up through the igneous rocks, up until the overlying sedimentary rocks. On the opposite side of the roadcut, the mafic dike is also seen, and the two can be traced to get an idea of the direction the intrusion spread across.

Both the overall igneous rocks and the mafic dike are truncated by the overlying sedimentary rock layer. The erosion of the igneous rocks and deposition of the overlying Lamotte Sandstone creates this 1 billion year gap.

Mafic dike (black, vertical feature) through the surrounding felsic igneous rock

The mafic dike is traced to this side of the street. As mafic rocks are more susceptible to erosion than felsic rocks, the mafic dike is eroding away and is seen as a vertical gap in the surrounding felsic igneous rocks. Atop both the dike gap and the felsic igneous rock is the Lamotte Sandstone, which is conglomeritic at the base, as evidenced in the picture.

Stop 5: Knob Lick Mountain and the Caldera

To wrap up what is going on geologically in this region, the next stop was up to Knob Lick Mountain, a lookout over the large caldera which has collapsed due to volcanic activity and pressure release.

Scenic overlook from Knob Lick Mountain. This point is along the rim of the caldera, as are the hills in the background. The lowlands are the caldera floor, caused from the collapse of the volcano from volcanic pressure release.

On the rim of the caldera. Lowlands in the near background are the caldera. Hills in the background are the continued rim of the caldera.

Field hat and hand lens, at the ready!

Stop 6: Silver Mines Recreation Area

The next stop, the Silver Mines Recreation Area, while also being a camping stop, was also chosen for its geology (of course). Next to this campsite is the St. Francis River and a former silver mine. A hike down to the river brings you across some of the local geology (more granite), but also contains more mafic dikes within the granite. This basalt demonstrates some interesting aspects of how a dike forms and cools, and was also part of a research project and GSA presentation by a fellow student.

Dam across the St. Francis River.

Silver mine across the river, along with a tailings pile containing lots of fluorescent minerals, along with galena and sphalerite.

The mine is normally accessible by walking across the dam, but not during this trip. A group of us hiked through the woods to this pile at night with black lights to hunt for the fluorescent minerals, with mild success.

Group up to learn about some geology

Irregular mafic dike in the granite.

Large mafic dike within the surrounding granite

A lesson in igneous intrusions within igneous intrusions.

Long day of geology = soak your feet in a nice stream atop some granite.

Getting dark. Time for dinner, then, hunting for minerals via black light.

Stop 7: Missouri Mines State Historic Site

The final stop of the trip was to check out the Missouri Mines State Historic Site. This is within the Old Lead Belt of Missouri, and constains a museum in an old mine mill complex from the lead mining days. There wasn't much geology to check out, but it was interesting to see and hear about the lead mining which used to occur at this site.

Stop 8: Back to Springfield, Missouri

Overall a good trip. It's nice to see some geology in Missouri which isn't limestone. A good combination of parks (with some information regarding the mining history of Missouri) and interesting field stops to hit some rocks with.

A few more scratches on the old rock hammer

Missouri AAPG Trip - Bennett Spring, Decaturville Impact, Ha Ha Tonka

The local American Association of Petroleum Geologists (AAPG) hosted a trip to check out some interesting Missouri geology. Destinations for this trip included (in order of appearance here on in) Bennett Spring, the Decaturville Impact Structure, and Ha Ha Tonka State Park.

Our first stop was in Bennett Springs State Park.

This is the location of the 4^th largest spring in Missouri, putting out about 100 million gallons per day (or about 150 cubic feet per second for those of you that are used to spring discharge in cfs). In comparison the springs I study around Springfield are usually less than 10 cfs. This spring flows from a conduit in the Gasconade Dolomite. Divers have descended down into this conduit for almost 200 feet before it was too small or flow was too great to continue.

If karst hydrology isn’t your thing, this place is a big fishing spot. Even in mid-January people were fly-fishing all throughout the park (ok, it was actually about 70 degrees outside still). I love fly fishing, so I’ll have to come back out here sometime with my gear.

This was all possible due to the trout hatchery on site which keeps the spring-fed river stocked with delicious catchable fish.

Because we are geologists, while enjoying the scenery from one of the bridges which crosses the river we all had to stop and look at the rocks which made up the bridge. One of the notable rock units was a rippled sandstone (the Roubidoux Sandstone), a local rock unit.

In one of the more obvious blocks we could see the ripples were nice and asymmetrical, while also being upside down (due to the rounded “crests” of the ripples, which are actually the troughs). I also took the opportunity to be creative with my hand lens.

Our next stop was to head to the Decaturville Impact Structure. This crater is a few miles wide and is only noticed in satellite imagery or by noting the unique structures in the sedimentary rocks (which are otherwise quite flat-lying in Missouri).

This crater is both recognized by its ring-shaped topographic signature…

The first roadcut is what most people refer to when they discuss the unique rock structures of the Decaturville Impact structure. Most people that study the rocks around Missouri know most of the sedimentary rocks here are basically horizontal. Structures, such as anticlines (at least obvious ones), tend to be rare. Here we see that the rocks are sometimes horizontal, then suddenly tilted, faulted, and folded at times.

Slightly dipping rocks.

Slightly more dipping rocks

Hinge of the anticline

More tilting rocks

Our fearless leader, demonstrating the thrust fault

Drag fold in the thrust fault (illustration below)

Much of the rocks have been heavily brecciated, almost to the point that referring to the in their original name and age is meaningless (geologic maps call some of these the Gasconade Dolomite, but it should really be said that the Gasconade is just the parent rock).

Breccia with large chert clasts

More breccia. Here, a layer of rock (gray) is broken and rounded at the edges

Clasts of granite were said to be found in the breccia, although we didn't spot any

Many of the clasts have been cored for paleomagnetics testing.

Large clast with paleomag boreholes, also in the surrounding matrix

More paleomag boreholes in this deformed layer

We drove further north into the impact structure and looked at some more breccias in the rocks.

Large clasts in the breccia

Strangely enough, large clasts of shale which now weather out giving the rock a porous appearance. How do you get football-sized clasts of loose, yet intact, shale?

Calcite vug

A strange sigmoidal feature with a clast in the center

Our third spot was to check out the "caprock" in the impact structure (assumed to be due to its undeformed nature while being in the center of the crater). It was a quartz sandstone-conglomerate, white to orange.

Checking out the sandstone/conglomerate

Some places are fairly mature but it gets coarse in some areas

Shot of one of the more mature spots through the hand lens

This sandstone was very sparkly

Some spots were very conglomeritic

After leaving the crater we had lunch and headed to Ha Ha Tonka State Park.

http://en.wikipedia.org/wiki/Ha_Ha_Tonka_State_Park

The first part of this spot involved visiting the "castle". At the park is the remains of a sort of castle-home built by Robert McClure Snyder from the early 1900s.

Little background story behind the ruins

A series of trails around the castle structure also provided some nice views of the steep valley where the spring is located in. We first explored the ruins, then went down into the valley.

This is the water tower to provide water to the castle

View of the castle from the river

Pointing off into the distance. Also, it was very windy

 

Map of the park. The photo above was taken at the red star.

Another map of the park with trails. We walked on most of the trails.

The spring, from above

The spring, again.

Spring-fed river

Some background of the spring. My favorite part was the name of the spring, Ha Ha Tonka, which translates to "laughing waters" by the Osage Indians. I found this fun because this same language is used a lot in names from my home state of Minnesota (Ha Ha, such as Minnehaha Falls in the Twin Cities, and Tonka is just everywhere in Minnesota, home of Tonka Toys, and my hometown of Minnetonka). All these words (haha, minne, tonka, sota, etc) can be combined to form a lot of words.

As explained by Wikipedia... "The word Minnesota comes from the Dakota name for the Minnesota River: Mnisota. The root mni (also spelled mini or minne) means, "water". Mnisota can be translated as sky-tinted water or somewhat clouded water. Native Americans demonstrated the name to early settlers by dropping milk into water and calling it mnisota. Many locations in the state have similar names, such as Minnehaha Falls ("waterfall"), Minneiska ("white water"), Minneota ("much water"), Minnetonka ("big water"), Minnetrista ("crooked water"), and Minneapolis, which is a combination of mni and polis, the Greek word for "city".

Illustration of the geology of the park. It was explained to be a very large collapsed cave/solution feature

The cliffs of insanity!

A natural bridge down in one of the sinkholes

Got back home while the sun was setting. Long day!