Monday, September 14, 2026

Dinos of Disney - Disneyland's Big Thunder Mountain

Disneyland's Big Thunder Mountain

My next entry in the Geology of the Disney parks is Disneyland's Big Thunder Mountain. I am specifying that this is "Disneyland's" version of the ride because even though the ride has been replicated three other times in parks around the world (two of which also have the a centerpiece dinosaur skeleton), this one is unique to Disneyland. 

Here is the setup for the ride from Disneyland:

Legend has it that after gold was discovered in the 1850s, eerie incidents took place in the mine. Trains would take off and race through tunnels… by themselves.

As you enter the cursed cavern, your train speeds up along the rickety track. Shoot under a booming waterfall and dodge a falling boulder from an unexpected landslide as you swoop around sharp turns and drop into desolate canyons.

On this rip-roaring adventure, you may learn that some legends turn out to be true...


For Disneyland's version of Big Thunder Mountain, the theme of the ride is based on Bryce Canyon National Park in Utah. Per The Imagineering Field Guide to the Magic Kingdom, this is distinctly different than the Magic Kingdom's version of the ride, which is modelled after Monument Valley. The reason for this is the aesthetics of the rocks. Monument Valley Tribal Park in Utah and Arizona is comprised mainly of sandstones and shales, making the color palette of Monument Valley to be very red and orange. 

Monument Valley Tribal Park in southern Utah

While the rocks found in Bryce Canyon are a much more pinkish "magenta" color, matching the aesthetics of the nearby Fantasy Land. And since Big Thunder Mountain butts up against Fantasy Land, the mountains were used as a visual backdrop to the land and the color palette was chosen to blend in. 

Bryce Canyon National Park in Utah

The upright spires within Bryce Canyon, called hoodoos, were also mimicked in the upper portions of the ride. You can see them below clearly above the primary dinosaur skeleton. The reason for the color palette of Bryce Canyon is because of the type of rock that it is. Bryce Canyon is predominantly made up of limestone, with sandstone and shale interbedded with it. The rocks were deposited during the Eocene in a large lake bed, forming what is known as the Claron Formation. 


The Claron Formation forms the Pink Cliffs part of Bryce Canyon and is broken up into two individual members: the Pink Limestone Member, which forms the reddish hoodoo rocks of the Pink Cliffs, and the slightly younger White Limestone Member. The White and Pink Limestone Members of the Claron Formation were deposited during the Eocene Period, approximately 60 to 50 million years ago. During that time, this part of Utah was covered by a vast lake, depositing thick layers of calcite that eventually consolidated into limestone. The Claron Formation also includes beds of siltstone and dolostone (like limestone but with dolomite instead of calcite). Limestone is also the same rock that caves form in because they dissolve in slightly acidic water


While the ride itself was meant to mimic the bedded limestones of Bryce Canyon, it is notable that along the path around the corner to the main entrance to the ride, the rocks there look distinctly sandstone. So much so that the Imagineers carved in cross-beds into the rocks themselves. Cross beds are geological features when dunes are essentially frozen in time and turned into rocks. When sand moves across the desert in a dune they climb up one side of the dune then fall down the steep edge, known as the slipface. This pattern of movement is then preserved in the dune as a cross bed. And depending on how the cross beds are eroded, they can form really cool patterns, such as is imitated in the ride. 


These cross bedded sandstones look amazingly like the sandstone beds of another national park located really close to Bryce Canyon NP, Zion National Park. Specifically the sandstones of the Navajo Formation, which is significantly older than that of Bryce Canyon's Claron Formation. 

Navajo Sandstone crossbeds from Zion National Park

The Navajo Sandstone is Early Jurassic in age, ~180 million years old. It is a very thick, ~1000 feet, eolian (desert) sandstone from an ancient sand sea known as an erg. This part of the ride likely stems from when this entire ride was built for Magic Kingdom, before parts of it were altered to fit in with Disneyland. 


An interesting addition to the ride is the very notable dinosaur skeleton, which is easily visible from the queue. While you are riding the ride you arrive here towards the end, where as you whip around the track, you eventually end up face-to-face with a dinosaur skeleton. At first glance, you would think this is a T. rex skeleton. At least, I believe that is what it is meant to be. 


However, looking closely at the skull, it appears ... off from an actual T. rex. Let's compare it to arguable the most famous T. rex, the Field Museum's SUE. Comparing the Big Thunder Mountain T. rex to SUE (pictured below), the biggest problem with the skull is the teeth. It's as if the designers tried to cram as many teeth as they could into the mouth, and all of the teeth are the same size and more rounded than real -life. Whereas, in the real skull the teeth are constantly coming to replace lost or worn teeth, so the size and spacing of the teeth differ widely within the actual T. rex's mouth. The overall dimensions of the fenestra (skull holes) are also smaller in the Disney skull than in the real animal. The nostril hole (the naris) is noticeably smaller, compared to the real skull, with everything getting a more boxy appearance, however I could attribute that to making the skull more durable with more surface area. 

SUE the T. rex from the Field Museum in Chicago

What I really wondered was where did the idea of this dinosaur come from. Was it meant to be a T. rex or something else. I find it really telling that the D23 post called "The Ultimate Dino-Tour of Disney Parks all Over the World" that goes over many of the dinosaurs in the Disney Parks just calls this "the bones of a dinosaur". No attempt was made at even naming the species, whereas they name the species of many of the other dinosaurs in the post.

Tony Baxter himself, designer of Big Thunder Mountain, stated that the dinosaur bones were meant as a tribute to the previous incarnation of the ride. Parts of the ride and theme were actually taken from the previous renditions of the ride called Rainbow Caverns Mine Train, which was then converted into the Mine Train through Nature's Wonderland. However, I haven't been able to find any pictures of any dinosaurs from those versions. The closest thing I could find, was that the second version mentioned dinosaurs during the ride, but that was about it. 

So although many Disney fans seem to have unanimously determined that this is a T. rex skeleton, Disney itself has shied away from denoting it as anything other than a "dinosaur".   


The location of these dinosaur bones is also suspect. If these bones are located in the "Bryce Canyon" portion of the the design, then they are clearly too old to be there. T. rex lived right up to the end of the Mesozoic, ~66 million years ago. The Claron formation is 60 to 50 million years old, which is too young. However the sandstone related formation on the outskirts of the ride is not the same as seen here with the bones in it. So perhaps this is meant to be a different limestone type deposit that underlies the Claron Formation and is therefore old enough to contain a T. rex?  

References
Wright, Alex. The Imagineering Field Guide to the Magic Kingdom at Walt Disney World: An Imagineer's-eye Tour. Disney Editions, 2005.

Friday, August 28, 2026

Geology of Disney - Disneyland's Matterhorn Bobsleds

 


Disneyland's Matterhorn Bobsleds

My next entry in the Geology of the Disney parks is Disneyland's Matterhorn Bobsleds ride. Based on the real Matterhorn peak in the Swiss Alps on the Italian-Switzerland Border, the ride was initially opened in 1959 and is noteworthy as Disneyland's first rollercoaster.  

Matterhorn Bobsleds looking towards the northeast from the direction of Main Street. 

Per the Disneyland website:
Matterhorn mountain certainly looks like its counterpart in the Swiss Alps— partially thanks to the excellent use of forced perspective. However, the peak is just a bit lower than the original—it’s exactly 100 times shorter than the 14,700-foot-tall real thing.

More than 800 gallons of paint were used to create heavier snowfall on the north-facing—just like the real Matterhorn. Glass beads on the façade glitter like actual snow!

Walt Disney fell in love with the real Matterhorn while filming the 1959 live-action film Third Man on the Mountain.

Back at Disneyland Park, Walt decided to cover a forested 20-foot-high mound named Holiday Hill with artificial snow, add a toboggan run and rename it Snow Hill. However, Walt always dreamed big, and the “hill” soon grew into a 147-foot-tall mountain. The attraction opened on June 14, 1959. 

Image of Matterhorn Mountain facing towards the southwest, looking at the east and north faces of the mountain. Image courtesy of MontBlancLines

When it was first constructed, Walt Disney had wanted the Matterhorn to look like it does from Zermatt, Switzerland, while standing on Main Street in the park. This means, however, that the ride is actually rotated compared to its real-life counterpart. When compared to different views of the ride and the mountain, it appears that the ride is rotated between 90 and 180 degrees from real-life. 

Looking towards the west at the eastern side of the ride.

Disney Engineers had then wanted the ride to resemble the actual mountain even more. So, during renovations in 2012, more snow was painted on the northern side of the ride, mimicking real-life. This is because due to the track of the sun across the sky, the northern side of the mountain gets less sun overall, and therefore less snow melts, resulting in greater snow cover. However, since the ride is essentially flip-flopped backwards, that means more snow was added to the wrong side, if you are looking at the real-life counterpart, but the correct side if you assume that the ride is placed correctly. That's confusing, I know. 



But, back to the geology. The real-life rocks that make up the majority of the real-life Matterhorn Mountain were formed 289 million years ago. They are a type of rock known as granodioritic orthogneiss and they belong to a group of rocks known as the Arolla Series. You can think of them as a type of granite. While the peak of the mountain is pre-Carboniferous gneiss, amphibolite, and marble of the Valpelline series, which are all metamorphic rocks. These rocks initially formed underground as magmatic intrusions within the region. 

Geological diagram of the Matterhorn Mountain. Image and following description from the Virtual Explorer. From top to bottom: mainly retrogressed kinzigitic complex of Valpelline series; coarse- to fine-grained and folded gneissic granitoids of Arolla series (GA), from Permian protoliths; Permian gabbro (G) with a thick mylonitic horizon (m) between them and at the base; basal slice of micaschists; calcschists (c), prasinites (p) and mylonitic gabbros (dark green) in the underlying Combin zone (Dal Piaz, 1992; Bucher et al., 2003, 2004).


These rocks were then pulled apart and pushed back together again a few times over the many millions of years, with the final time around 65 to 50 million years ago during the Alpine Orogeny. The Alpine Orogeny occurred when the African continent crashed into the European continent, jumbling rocks from multiple different continents together and forming the Swiss Alps. This layer cake of rocks results with African Crust, Oceanic crust, and European Crust all interbedded, forming the Matterhorn structure as seem in the diagram above. 

"Rocks" on the western side of the Matterhorn Bobsleds. 

Pictured above and below are the "rocks" on the western side of the Matterhorn Bobsleds. While they are clearly painted representations of rocks, they are likely meant to represent the Arolla Series granodioritic orthogneiss. Again, just think of them as "granites". A closer look at these "rocks" are below:


The fracture of the rocks and the speckled pattern of the rockwork, clearly show at least some resemblance to details for the Matterhorn Mountain itself, however it is clear that these "rocks" would never pass the test as something that is actual rock. After the rocks were formed, and then jumbled together, creating the Swiss Alps Mountains as a whole, they were then slowly eroded over time. 

View of the Matterhorn Bobsleds looking roughly towards the south.

This erosion has ramped up over the last 2+ million years, where glaciers had been slowly eroding the mountain peak until only the feature that we know of as the "Matterhorn" remained. This type of geological feature is actually known as a "horn". In geology, a horn is a "high pyramidal peak with steep sides formed by the intersecting walls of three or more cirques, e.g. the Matterhorn" per the Dictionary of Geological Terms. A cirque is a "deep, steep-walled recess or hollow ... situated high on the side of a mountain and produced by the erosive activity of a mountain glacier."

Although I have seen people referring to the Matterhorn as a "karling", which is a geological term I had been unfamiliar with (and one not in my dictionary). Per Huguet (2023), a karling is an "angular peak, with steep walls and sharp ridges, undercut from all sides by glaciers". This seems just a game of semantics to me, but most of the definitions of a horn used the Matterhorn as their "type" specimen, so the Matterhorn has to be a horn, by definition. But that's just my opinion. 


A "cast of a footprint" displayed alongside the Matterhorn Bobsled ride

Alongside the ride there a cast of a footprint which states that it is a "Cast of footprint discovered by Matterhorn expedition south slope, May 27, 1978." This was clearly added after the creation of the ride almost 20 years earlier. While I can't confirm exact placement of this cast of a "trace fossil", it appears to have been added during the 1978 refurbishment of the ride which included the animatronic yeti, Harrold. 

Enlargement of the sign set below the "footprint cast"

While obviously a fake, this does bring in the element of trace fossils into the discussion. Per one of my previous posts "What are ... trace fossils?"

[Trace Fossils} are basically what an animal creates as it does stuff. Stuff can include walking, burrowing, sitting, eating, living, etc. Whenever an animal interacts with the world around it, it leaves evidence, a trace if you will. These traces are what I study. They are not the actual animal but sometimes are found in association with the animal. The easiest way to visualize this that I can think of is with footprints in the snow (as seen below). Footprints are the most basic type of trace fossil. They illustrate locomotion of an organism, whether it is a human, a rabbit, an insect, or anything in between.

And this footprint cast also reminds me of the footprints found alongside Gertie in Animal Kingdom.


So, while it is ancillary to the geological description of the Matterhorn, it does as an interesting wrinkle in the story of the ride.

References

Thursday, August 13, 2026

Geology in the Wild - Adirondack Mountain Reserve

Back in January of 2022, we were invited for a winter hike within the Adirondack Mountain Reserve, and while we had a fantastic time, there is something more important underfoot that needs to be discussed. And that is the geology! 


Gates to the Adirondack Mountain Reserve. Photo by Gwendolyn Craig from Adirondack Explorer

The Adirondack Mountain Reserve (AMR) is a small park located within the larger Adirondack Park near the small town of Keene, NY:

Location map for Adirondack Mountain Reserve (from the NYS DEC)


Per the AMR website:
The mission of the Adirondack Mountain Reserve is to preserve and protect the forests, lakes, mountain streams, and wildlife on our wilderness tract for the enjoyment of our members and, under the terms of a Conservation Easement in perpetuity to the State of New York, members of the public. We will preserve the forever wild character of this forest land and our property at St. Huberts in a manner appropriate to allow the enjoyment of their wilderness beauty. The mission also includes the operation of a club, with associated facilities, for the pleasure and respectful recreation of its shareholders. 

Adirondack Mountain Reserve map. A digital version can be found the New York Almanac 

The park essentially starts in the northeast with the East Branch Ausable River valley. The entrance gate is located along this northeastern border of the Reserve. The park follows the river valley to the southwest through the Lower and Upper Ausable Lakes with another unnamed lake (or at least a lake I can't figure out the name of) situated at the southwestern point of the reserve boundaries. 
Map of the park with some notable points highlighted.

There are several spots within the park where the geology of the region can easily be seen. However, since we were there in winter, even those locations had less than ideal exposures. These spots that we stopped at are highlighted on the map above.

Beaver Meadow Falls

Hiking southwest from the entrance gate one of the first locations that you can see the geology is at Beaver Meadow Falls. Waterfalls are always a great place to check out the geology.

Rainbow Falls

Continuing towards the southwest along the trail, you then come across Rainbow Falls.

Indian Head Vista

And eventually you can make your way up to the Indian Head Vista, with an absolutely gorgeous view of the Lower Ausable Lake. 

View of the rocks on the Indian Head Vista. 

Pictured above are the rocks at the vista itself. However, if we look at the geological map below, it can be noticed that almost all of the rocks within the Adirondack Mountain Reserve are actually the same rock. They are nearly all the orange color, which is denoted as "a" on the Geological Map of New York

Geological Map of of the Adirondack Mountain Reserve. The black box indicates the extents of the map pictured above. 


Reading the Legend from the New York State Geological Map itself, I warn you, there is some heavily geological terminology in the paragraph ahead. Per the Legend, the rocks within the park, denoted as "a", are:
Black to light gray or greenish-gray metanorthosite and anorthositic gneiss (Marcy facies); overprint signifies mafic mineral content in excess of 10 percent (mainly gabbroic or noritic metanorthosite and subordinate anorthositic metagabbro or anorthositic metanorite-Whiteface facies). Subordinate members of this series grade through metagabbro or metanorite, to ilmenite-magnetite-rich metagabbro or metanorite, to pyroxenite rich in ilmenite-magnetite, to ilmenite-magnetite ore. Primary subophitic texture is variably destroyed by granulation and recrystallization resulting in a crystalloclastic fabric. Metamorphic minerals include garnet, clinopyroxene, quartz, hornblende, and a plagioclase less calcic than the original. Mafic mineral percentage is contoured in northwestern portion (St. Regis Quadrangle) of the Marcy Massif, contour value being shown on high side of contour line. 
While that is a lot of technical jargon, I will try and break it down. The rock unit that the AMR sits on it known as the Marcy Anorthosite Massif, named after Mount Marcy, the highest point in NYS, which is located just to the west of the AMR. Anorthosite is an igneous rock made up almost entirely of the mineral plagioclase feldspar. And not only does this rock body cover the park, it is massive in size.

Large view of the Adirondack region of New York, showing the full extent of the Marcy Massif. 

Typically when we have mountain, we expect the geology to be jumbled up with many types of rocks overlaying each other. And that is actually what we see for the most part, outside the orange colored Marcy Anorthosite Massif. The Marcy Massif though sits at the center of the mountains, and it is in essence, the core of a dome structure that makes up most of the Adirondack Mountains.

The core of the Adirondack Mountains, the Marcy Massif, is ~1.1 billion years old (Ga), and covers an area of 3000 square kilometers (~1150 square miles). The rock was initially formed as an igneous intrusive magma body that cooled slowly over time, forming the plagioclase rich anorthosite. After formation this rock underwent periods of metamorphism where parts of the rock were altered, mostly along the outer edges. That is a lot of what is in the description of the rock unit above. These metamorphosed regions have various amounts of minerals that are specific to metamorphic rocks.

Cross section of the Marcy Massif across the Adirondacks. Image courtesy of Regan et al., 2019.
The formation of the Adirondack Mountains is where the unique status of the Adirondack Mountains comes into play. While many people may think that the Adirondack Mountains are just a subsection of the longer Appalachian Mountains, they are, in fact, their own distinct set of mountains. The Appalachian Mountains formed when North America slammed into Africa, forming the supercontinent Pangea, and lifting those mountains upwards as a result of the collision around 300 million years ago. Since the breakup of Pangea, these mountains have generally remained inactive and have been slowly eroding away over time. While the core of the Adirondacks formed during the Grenville Orogeny, over 1 billion years ago, the mountains themselves started to be uplifted ~20 million years ago. The reason for this uplift is currently unknown but the result was a dome structure with the Marcy Massif in the center. The way that domes form, it causes the younger rocks to erode away from the central area of the dome due to fracturing experienced during the uplift. This fracturing and erosion is the reason we have some of the oldest rocks in the Adirondacks exposed in such a huge degree. 

The result is that the AMR sits near the center of a massive dome structure, comprised almost entirely of some of the oldest rocks found within the Adirondack Mountains and there are plenty of places within the park to check them out. (Note: there are some slightly older rocks found elsewhere in the Adirondacks, but not nearly as notable as the Marcy Massif.)

Tuesday, June 16, 2026

Geology of the National Parks in Pictures - Cuyahoga Valley National Park

My next post about the Geology of the National Parks Through Pictures is from a trip to Ohio shortly after we moved to New York for a memorial service for my dear friend Dale.


You can find more Geology of the National Parks Through Pictures as well as my Geological State Symbols Across America series at my website Dinojim.com.

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Obligatory entrance sign shot.

Cuyahoga Valley National Park is actually a rather large park with many things to do and places to go within the park. It is essentially an urban national park, sitting just outside of Cleveland and Akron, Ohio. Since our time within the park was limited and we could not do everything possible, we decided to do a hike up to Brandywine Falls and take a train ride through the park.

Brandywine Falls

The hike up to Brandywine Falls and the falls themselves show a wonderful cross section of the geology available within the park. As you can see in the image of the falls above, there are three main rock formations within the park. Starting with the bottom, and the oldest, is the Cleveland Shale, which sits at the base of the falls. The Cleveland Shale is Late Devonian in age (~350 to 400 million years old) and is mostly a black shale, meaning that it is rich in organic material (e.g. oil and gas). The Cleveland Shale is assumed to have been deposited in a fairly shallow water environment with low oxygen levels. These low oxygen levels have led to the preservation of a number of fossils within the formation including 22 species of jawed fishes, including the 40 foot long Dunkleosteus, and one of the earliest known sharks, Cladoselache.


Sitting above the Cleveland Shale, and encompassing the majority of the height of the falls, is the Bedford Shale. The Bedford Shale is also Late Devonian in age (~350 million years old), and represents a shallowing of the water that was in the region. The rock units are interbedded shales, siltstones, and sandstones that progressively get more sandy as you work your upward through the unit. A large amount of these deposits were laid down within river deltas that meandered back and forth across the region. These interbedded deposits are what give the formation the multiple thin beds as seen in the close up above. The Bedford Shale rocks are what creates the rock wall along the edge boardwalk trail towards the falls (pictured above). 

Downward view of Brandywine Falls

The uppermost layer that comprises the falls, and the capstone of the falls, is the erosion resistant Berea Sandstone. The resistance to erosion of this layer is what created the falls in the first place, preventing the breakdown of the much softer layers below (the Bedford Shale). The Berea Sandstone is also Late Devonian in age (~350 million years old), and continues the environmental shallowing seen in the lower Bedford Shale. The Berea Sandstone is made up of interbedded sandstones and siltstones, with mostly sandstone, that were deposited just offshore within the deltas of nearby rivers. This sandstone, because of the porosity of the rock (gaps in between the sand grains), makes this formation a valuable oil reservoir, when found deeper underground.  


There are a few other geological formations within the park, most of which are related to the glacier deposits from the Ice Age, ~2 million to 10,000 years ago. However, we didn't see most of those. We were able to take a train ride along the Cuyahoga River, which makes its way across the entire park. Our train ride took us along the river for pretty much the entirety of the trip and it was definitely running very high/flooding while we were there. While the picture above you can't see how high the river really is, the picture below shows a little better the full extent of the water levels. The ancestor river to the Cuyahoga River first began to form 150 million years ago and continued to erode down into the landscape forming the prehistoric river valley until the glaciers damned up the river and filled that ancestral valley with till, i.e. glacial sediment.  


As the glaciers started to melt away, the Cuyahoga River was reformed as a glacial outwash stream, flowing south away from the current Lake Erie. Due to the topography of the landscape, and despite the glaciers being towards the north blocking the way, the river still wanted to flow towards the direction of modern day Lake Erie. As this new Cuyahoga River carved down into the landscape as a glacial outwash stream, it eventually hit the topographical high around the city of Akron. When it hit this high it also rediscovered the ancestral river valley and was able to excavated the glacial sediments within it. Within the ancestral valley, the course of this new Cuyahoga River was redirected back towards the north from the City of Akron in a big U-shaped bend. This bend is what has caused the river to be known as the crooked path. Even the name of the valley is derived from what the Native Americans named the river, “Ka-ih-ogh-ha”, meaning crooked. 



Alongside the river, the Ohio & Erie Canal was formed back in the 1800's and maintained through the early 1900's. This canal route contained several locks used to raise and lower boats along the waterway. Lock 29, along the Cuyahoga River, is a former Ohio & Erie Canal lock where the original construction sandstone blocks can still be seen. All the other locks had their sandstone blocks replaced in the early 1900's when their sandstone blocks had deteriorated. However, Lock 29 had it's masonry redone in 1882, and therefore the sandstone blocks were still in good condition during the renovation of the other locks. Therefore, while all those other locks were converted to concrete, we still have the original sandstone here. The sandstone used for these locks was the aforementioned Berea Sandstone. Because it could be quarried locally and was extremely durable (hence waterfall), it was chosen as the ideal rock to make the lock out of. Blocks of sandstone were taken from the nearby Deep Lock Quarry less than 2 miles away.

References

Thursday, May 28, 2026

Geology of the National Parks in Pictures - Herbert Hoover National Historic Site

My next post about the Geology of the National Parks Through Pictures is from our move across the country from Utah to New York. Along the way we visited 13 National Parks as well as some other sites. This was the 13th, and final, National Park along the way.


You can find more Geology of the National Parks Through Pictures as well as my Geological State Symbols Across America series at my website Dinojim.com.

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Obligatory entrance sign photo


Herbert Hoover is notably the only geologist (to date) to have become president. His wife, Lou, was also a geologist, and the first woman to receive a geology degree from Stanford University. And while you would hope that a geologist would have many geological tidbits around his National Historic Site, there are not many across the park.

Schoolhouse

In front of the schoolhouse there is a sign that has a little geological tidbit about Hoover. It is assumed that Hoover attended school here from age 5 until ~10 or 11, after which he went to live in Oregon with his uncle after he was orphaned. Eventually, he attended Stanford and received a degree as a Geological Mining Engineer, with the photo in front of the school house here, showing Hoover as part of a geological survey squad in 1893.

Herbert Hoover Birthplace Cottage

Another site within the park, the Birthplace cottage, has some geology to it. The foundation of the birthplace cottage had been changed over the years, with the original foundation having been constructed using local boulders found on the prairie. The cottage was then purchased by another family and moved in 1889. However, it was then restored to its original location in 1934, when the Hoover family repurchased it. The stones used for the current foundation is a "local stone", however I can't find any more information on the specific rocks used. My guess is that it is a dolomite (a type of limestone), because the park sits upon several dolomite formations.

Geological map of Herbert Hoover National Historic Site and surrounding area. Image courtesy of the NPS.


The majority of the park sits upon the Silurian Age (~430 million years old) Scotch Grove Formation and the ~425 million year old (still Silurian) Gower Formation. Both of these are fossiliferous dolomites that formed in fairly shallow marine environments. These rocks are slightly younger than the bedrock below the nearby Effigy Mounds National Monument. If the stones for the birthplace cottage were quarried locally, it is likely that one of these two formations were the ones quarried. 


One of the most notable geologically related construction stones are the marble slabs used for the grave markers for both President Hoover and his wife, Lou. The marble slabs are noted as "Vermont white marble", however there is little information besides this to identify the quarry, region, or formation of the marble use. It is assumed that, due to the time period that these slabs would have been quarried, and the importance of the memorial (being a former president) that these are likely from the Danby Imperial quarry.


The Danby quarry is the largest underground marble quarry in the world. This quarry, located in the northeast flank of Dorset Mountain in Vermont, mines the Columbian member of the Lower Ordovician Shelburne Formation (~480 million years ago). These marbles were originally deposited as a limestone within a shallow marine environment. Then burial under other rocks and metamorphism from mountain building heated the limestones up and folded them, altering the minerology to produce the marbles as they are today. Blocks of marble from this quarry have been used in the New York Public Library, the Jefferson Memorial, Harvard Medical School, the U.S. Senate Building, Arlington National Amphitheater, the Supreme Court, and the United Nations building.


Although it is possible to find some of the bedrock along local stream channels, the majority of the bedrock within the park is located fairly deeply beneath glacial sediments (hence the original boulders used for the birthplace foundation) that were deposited during the early and middle Pleistocene Epoch (about 2.6 million years ago to 500,000 years ago). These glacial deposits are known as the Pre-Illinoian Alburnett and Wolf Creek formations, which comprise mostly of till, a glacial deposit that is essentially a clay rich mishmash of everything that can be thrown into one pile. Think of a glacier scouring the surface of the earth and then just dumping everything it picks up into a pile like a conveyor belt. That is till. 

References