We camped along a creek in Silverton across from a silver mine and mill, as shown in this satellite image; the mill is indicated by a white triangle. The mine and mill are now open for tours but I didn’t have the opportunity to visit them.
Here is a photo of the mill. The mine went into the mountain behind the mill, which appears to be a fault. Veins of silver and gold are frequently found along faults, which are weak lines in the crust where the high-pressure fluids can penetrate. Silverton was settled in 1874 and had a peak population of 5000 in the early 1900s. The mill is nestled against the ridge south of town.
Gold and silver milling technology was changing rapidly while Silverton was active but this mill probably first used an “arrastra” method with a horse (or maybe water power) to drag a heavy stone around a central post to crush the ore brought from the adjacent mine shaft. Water and chemicals like mercury would have been mixed with the crushed ore to form an amalgam (silver/gold plus mercury), which was heated to boil off the mercury. It is likely that this inefficient method was replaced with a Comstock mill, which used a heavy piston to crush the ore and a cyanide process would have been used to extract gold more efficiently.
After leaving Silverton, we headed west toward Ophir Pass (see photo above) where the landscape changed dramatically. This photo shows the view looking west from Ophir Pass; note the lack of vegetation in this rocky terrain. It would be extremely difficult for trees or shrubs to take root, or for lichen to grow on these constantly shifting fragments of the original volcanic rocks. It is noteworthy, however, that grass is growing at this same elevation in the background where the rocks are not as fragmented.
Note also the muddy matrix supporting the trail, which implies that these rocks contain minerals that weather rapidly to form clay, i.e., these rocks comprise much more Ca-bearing feldspars like plagioclase rather than the K-feldspars we saw early in our journey, which form gravel. This next photo shows that these rocks are very resistant to erosion where they are less fractured.
As an aside, this kind of scree is impossible to climb in a wheeled vehicle, and off-roaders avoid it like the plaque. There is no cohesion amongst these fragments and our tires just churn it up like water from a paddle wheel; of course, with enough horsepower and large enough tires it can be climbed but not consistently.
A close-up view of one of the larger fragments shows that this rock can be classified as an andesite porphyry.
The lighter colored cobble is a piece of host rock and not a mineral crystal. Zooming in shows many smaller particles of rock (not mineral) and an irregular surface texture that suggests a squeezing of the ash as it was deposited from the air and compressed as it cooled.
We continued traveling eastward until we encountered some sedimentary rocks containing sandstones and layers of coal. I have no photos of these formation however, but according to the USGS geologic map these are Cretaceous (85-60 mya) Mancos Shale, a nearshore marine deposit with coal beds, which probably contributed to the naming of Black Mesa. We chose a camp site among the Tertiary intrusive rocks as indicated by location 6 in this image.
Our campsite, among spruce and aspens, was apparently used by hunters and boy scouts. Here is a photo that includes a generic hand sample of an andesite and a 15x photo of a sample from our campsite.
The rocks (there were no exposures where we stayed) looked like this andesite porphyry from geology.com. The larger photo shows that the hand sample color of grey is probably caused by the areas of grey glassy material, which are not likely to be quartz as in the granites we saw earlier because quartz is not present in intermediate igneous rocks like this. The best general reference to understand the rocks where we stayed is the Roadside Geology of Colorado, suggests that intermediate intrusive magmas penetrated into the thick sequence of volcanic rocks to form diorite with unusually small grains because of rapid cooling so near the surface.
Here is another 15x photo of this rock from our campsite. This is a 15x magnification of a rock fragment at location 6.
If this hand sample had been light colored, the area indicated by circle A would be reasonably interpreted as quartz, as we saw in the sample from the Wet Mountains and the Sangre de Cristobal Mountains. However, the overall grey color of the sample, and the evidence of crystal terminations in A suggests to me, as a field geologist, that these are actually plagioclase feldspar with more Ca than Na (i.e. the more Ca the darker the plagioclase). Circle B is focusing on the white crystals that, though small, are clearly crystalline and not glass. These minerals are interlaced with the darker crystals and thus I interpret them to be a more Na-rich plagioclase feldspar (Na and Ca plagioclase form a continuous spectrum in this mineral). Area C shows a crystal of a dark mineral with much smaller crystals embedded or adjacent to it. I cannot tell if this is pyroxene or amphibole (a pyroxene-like mineral with water included in its crystal structure) but both contain Ca as well as Mg (magnesium). The most ambiguous (to me) mineral is indicated by circle D, which highlights an orange crystal; we saw pinkish to orange K-feldspar in the Proterozoic granites from the Wet Mountains but there should be no potassium in an andesite. However, some combinations of Na and Ca in the plagioclase series are this color and it is reasonable to assume (lacking thin-section analysis) that this is another phase of these common minerals.
If we estimate the composition of this sample as we did for the granites discussed in a previous post, we get the following: Ca-plagioclase = 50%; Na-plagioclase = 35%; mixed-plagioclase = 10%; amphibole = 5%. The fact that we can see crystal structures even in the smallest minerals in this sample suggests that this is one of the rapidly cooled diorites from the area rather than an andesite (volcanic), which would not have visible crystals at less than 100x magnification (e.g. under a microscope). The grey areas, in other words, are not glass by very small crystals formed near the surface.
We see the end result of this in the following photo of a local muddy area, where it was almost impossible from sliding sideways into the ruts.
As mentioned in previous posts, minerals containing Ca weather rapidly and produce by-products like clays that form MUD; however, as we saw later in our travels, when these clays form a veneer over subjacent regolith, they can be negotiated with care.
After passing thru the narrow canyon along Mill Creek (see previous post), we spent the night at Deer Lakes in Grand Mesa-Uncompahgre-Gunnison Natl Forest before ascending the lofty passes of the San Juan Mts. It stopped raining long enough to set up camp and then continued intermittently throughout the night and next day.
We continued deeper into the middle phase (30-26 mya) volcanic rocks and the outcrops became darker colored, reflecting the chemical evolution of the magma source for these ash layers and flows. This general area is indicated as site 5 on this photo.
We continued following wide gravel roads and paved highways until we reached Lake San Cristobal (elevation 9000 feet), where the resistant welded tuffs and flows produced by this volcanic phase formed peaks such as this one overlooking the lake.
The road followed money to Lake San Cristobal, where condos are everywhere and there is even a marina with small sailboats and row boats. The pavement and new gold (money) stopped at the inlet to the lake, where Upper Lake Fork Rd became a single lane gravel trail with intermittent wide spots to let opposing traffic by.
There was a lot of traffic heading back to the lake because the trail eventually encounters andesite flows that form ledges that a bulldozer could not level. Cars were not going to Cinnamon Pass, which is where we ended up.
Here is a photo that suggests why there is a road to Cinnamon Pass and beyond. I snapped this image while trying to avoid going over the side, but it shows a vein of what is probably pyrite (fool’s gold) in the cliff overlooking the Gunnison River.
Cinnamon Pass was the second highest elevation we reached during our trip (12640 feet). The peaks, which weren’t much higher, were composed of the alternating layers of ash and lava flows. These photos show the appearance of these rocks; note the small angular shards that litter the slopes. These result from dense joint patterns that indicate extreme brittle deformation, probably from faulting that followed volcanism continually.
The headwaters of the Gunnison River ended in a shallow, flat meadow that appears to be another cirque (glacier origin area) from the recent ice ages. After crossing Cinnamon Pass, where the horizontal rain and fog/clouds made for miserable conditions, we dropped down into Animas Forks, which must have been a bustling mining community at one time. Today, however, it is represented by a few old mines (some for sale) and a USFS toilet.
This is where the road from Lake San Cristobal led. Apparently, these mines produced enough gold and silver to justify the road we followed to California Pass (elevation 12930 feet). There was snow on the ridges and their concave shapes suggests that glacial erosion was a significant factor here.
Note the sharp edges along the ridge, and the tilting of the bedding planes (original horizontal surface upon which the ash flows and lava were deposited); faulting was ubiquitous over the several million years during which middle phase volcanism took place. This was followed by the late phase volcanism associated with the Rio Grande Rift, which was discussed in the Prologue.
This image shows the irregular surface of the San Juan Mts but it cannot prepare you for the 3000 foot descent that lies ahead on the trail to Silverton.
I saw several veins of what looked like K-feldspar as we began our descent, such as this one that had not been explored by miners.
Further on, I noticed this area that had been dug in an exploratory manner but apparently it did not look promising.
This vein is more promising from an economic geology standpoint because it appears to contain much more quartz, which is associated with the last stage of magmatic fractionation that produces fluids high in elements that don’t fit well into most silicate minerals (e.g. gold, silver, rare earths).
It would appear, however, that none of these veins west of Animas Forks contained economic concentrations of gold and silver. We made our final descent to Silverton via the potentially deadly Corkscrew Gulch trail in the rain, which is why I have no photos of the trail or the rocks. As we approached US-550, the hills were dominated by light-colored talus that did not originate from mines, but from weathering of the volcanic rocks. This could be another example of dense fracture patterns associated with faulting after the original ash flows were deposited.
We camped at Marshall Pass (location 3 in the photo below) among what we thought were Aspens, which apparently like the rocky soil that probably originated from weathering of the shales we saw in the previous post. The rocks were angular and uniformly about 8 inches in length; their size and shape are consistent with the origin of Poncha Creek following a fault through Marshall Pass. I will discuss this later.
After descending from Marshall Pass, we followed some the TAT until we entered the San Juan volcanic field. Our route took us into the early phase of this volcanic period in CO’s history about 35 mya, when volcanoes in this area were producing large amounts of ash and a lava similar in composition to the granites we have seen in previous posts. This photo shows the sudden appearance of such a volcano as we entered the San Juan Mts.
Note the rounded ridges and small peaks around the base of the main cone. The ridges are weathered lava flows, which often originate from the bottom of volcanoes and the small peaks are evidence of minor eruptions around the base of the main volcano. The flows are more visible in this photo that shows several such flows. We had the opportunity to follow a trail along one such flow, which still formed a scarp that is ~5-15 feet high after 30 my of erosion.
This photo shows one of the many well-preserved cones from the early phase of volcanism.
These volcanoes were producing mostly ash and debris that formed immobile layers that did not flow; however, they also produced ahs flows like Mt. St. Helens that would have moved rapidly down the slopes and destroyed anything in their path. These photos were taken at the approximate location indicated as “4” in the base map below.
I have some photos of these rocks that show some of the textures of these volcanic layers. This photo shows a tuff that does not appear to have melted together after the material was deposited from the air. If the fragments are hot enough and are buried under later volcanic material, they can become fused to form a “welded tuff” but that is not the case for this sample.
It has the coloration of the orthoclase (K-Feldspar) we saw in the granitic rocks from previous posts but it also has many holes (vesicles), which originally contained gas that later escaped; some of these holes are left from weathered minerals and rock fragments that were entrained during eruption. I suggest using your browser to zoom in on this image to see the remarkable number of different particles it contains, many of which are probably from the sedimentary rock through which it passed during extrusion. Here is another sample that has a different weathering color but is essentially the same.
The bulk of these tuffs is silica glass that didn’t have time to cool and form quartz crystals; it is about the same as the glass we produce for windows. I think I should again suggest that anyone looking at this post should click on these photos and zoom in with the browser to appreciate their composition.
The next photo shows a sample with easily identified quartz (the gray areas) and areas that show one of the weathering products, as shown by the white coloration. My first guess about the white material is a salt or carbonate formed from rapid decomposition of the glass to release common rock elements like Ca or Na, which formed minerals like NaCl (salt) or carbonates like calcite (CaCO3); possibly with metals included, e.g., Fe or Mg. Only laboratory analyses can identify these weathering products as well as the particles included in the original tuff.
This photo shows what an exposure of these tuffs looks like. Note the cliff at the top and the substantial debris at its base because of erosion of these relatively weak ash flows.
As we travelled to the SW, however, we entered a region where volcanism occurred several million years later, the middle phase of volcanism in the San Juan Mts. These volcanic rocks include layers of more resistant lava and welded tuffs. Here is a photo of a canyon formed from mixed layers of tuff, welded tuff, and lava flows.
The nearest outcrop also shows what could be termed a volcanic breccia because it contains large (~12 inch) cobbles in a fine-grained matrix. This photo also shows the variability of the different flows in the cliff. Note the irregularity of the layers as if they were being deposited on an eroded terrain.
As a volcano releases pressure and material from a magma chamber, a number of different types of effusives are produced; for example, we have just seen examples of tuffs that are formed from exploding liquid magma and any material it picks up as it exits the magma chamber thru channels in the rock. Here is an example of a tuff that appears to have been so hot that this liquid rock melted together to form a welded tuff.
Again, I urge the reader to zoom in on this photo, which shows fewer and smaller vesicles, as well as a layering and white minerals that I cannot identify from the photo.
The previous hand sample shows obvious layering but no evidence of flow; i.e., this material was deposited from the air and formed separate layers, possibly over a short period of time (e.g. days to weeks). I think this because there is some evidence of mixing between layers, which would not occur if it flowed or solidified between layers. This relationship is better seen in the following photo, which shows a kind of settling of an upper layer into a subjacent one.
There is no geologic reason to expect to find useful minerals (valuable) in these volcanic layers because they do not show any evidence of veins or remineralization like we saw on the previous post. Nevertheless, as we passed thru the flows of the middle phase, we crossed “Mineral Creek”, which was an opaque green as it flowed from the adjacent mountains. I stopped and took a panoramic photo of the valley and zoomed in on the opposing hills to discover an interesting symmetry across the valley.
The panorama photo has white outcrops circled. The lower photos show close-ups of the opposing sides of the valley; similar exposures occur on both sides of the valley. These volcanic layers are horizontal and there is no obvious faulting (e.g. dipping layers). There were no trails to either exposure so any mining reconnaissance did not suggest economic remineralization (i.e. gold or silver) worth road building. Until I can find the time to collect samples from both exposures and compare them, this remains a geological mystery to me.
I have a footnote to this post. We drove the dirt roads in this area under both wet and dry conditions. The roads were all wide and smooth with very little washboard texture but they created a lot of dust when dry. Weathering of the tuffs produces silt-sized glass particles that drain moisture fast but stay in the air when disturbed by truck tires, especially offroad tires. It was quite different than the gravel roads we encountered in the Wet Mountains and at Marshall Pass, both of which were based on weathered granitic rocks that produce sand grains as they erode.
We camped the first night in the Pike-San Isabel National Forest at the northern end of the Sangra de Cristo Mtns., after passing some large greenhouses filled with shrubs, either tomatoes or marijuana but probably the latter (legally grown in CO). The neighbors were all friendly as they drove by our camp site shown at location 2 in this map.
We set up in a borrow quarry for road repair soil, which was surrounded by granitic rocks similar to those seen in the Wet Mountains, but looks can be deceiving. Here is a photo of the exposure at our camp site.
I attached the 10x lens to my iPhone and took the following photo, which we will now examine.
The K-feldspar (orthoclase) is the orange mineral; it comprises about (estimating from the photo) 30% of this sample. The Na-Feldspar (albite) is the white mineral, which is about 20% of the sample, and quartz (mostly gray and pinkish in this sample) is about 40% of the sample. I would estimate that amphibole (the dark mineral; however, some of this may be other minerals that could only be identified by thin section analysis with a microscope) is about 10% of the sample. I cheated to make them add up to 100% but the errors won’t matter when we compare it to the sample from the Wet Mts shown in the last post; that sample was approximately albite = 7%; orthoclase = 50%; quartz = 40%; and amphibole = 2%. Even taking account of my errors in estimating their composition, these rocks are very different; they are also very different in age. The Wet Mts sample is ~1.5 by old whereas the Sangre de Cristo Mts rock is less than 70 my old. We will discuss this in a later post. This young age comes from the USGS CO geologic map with data sources, which lists the rocks at site 2 as Laramide Granitoid.
We crossed through the intermontane valley and the town of Salida before following Poncha Creek to Marshall Pass, indicated by location 3 in the previous photo. This was a steep rise to an elevation of 10842 feet, with a great deal of blasting, cutting and filling of deep ravines in the surrounding peaks. This leg was interesting because it took us to the Continental Divide, which separates eastward-flowing rivers from those that flow westward. It also is not within a single mountain range but instead separates the Sawatch Mts to the north from lower hills to the south.
This area also includes some of the host/country rock that the granitic rocks were intruded into. This photo shows an exposure of the host rock for the granitic intrusions at the southern end of the Sawatch Range.
This photo shows the orientation of the original bedding plane (horizontal surface of the sediments that became the rock before it was metamorphosed and intruded) of the silts and clays that were originally deposited during the Tertiary period (~65 – 2.5 mya). The tilting occurred during the Laramide Orogeny that created the Rocky Mts. The circle shows where the following photos were taken.
This first photo is at normal magnification; it shows striations on the bedding plane (indicated by black lines) that are probably from sliding during movement, overlaid on original bedding plane irregularities.
I have to admit, however, that there is always some uncertainty when only examining one exposure; many geologists have examined this region and I am implicitly including their conclusions in my discussion. When we examine the next photos, which are at 10x magnification, we can rely on our own judgement.
When we are examining igneous rocks that were crystallized from a relatively uniform temperature and composition, we can assume a lot, as I have been doing up until now. This photo shows some of the intruded rock within a few feet of the tilted rocks shown in the previous photo. I have circled regions of this small image (~1 cm in diameter) that would be of great interest to an economic geologist. I can only state with some confidence that this sample has a lot of orthoclase (reddish colored) and several different minerals that formed within small cavities when the intrusion occurred. Only microscopic study could positively identify the white mineral (albite?), the elongate crystals (orthoclase) and the very small dark minerals (pyrite?). I use question marks because these aren’t even guesses.
I took a closer look at one of these thick veins near the host rock with the 15x magnification lens to see if it would help.
The quartz is easy to identify from its gray hue (in these samples) but the circled area could be pyrite, which is also known as “fool’s gold”…where there is smoke, there’s fire…
This photo at 15x magnification shows a bleb (tiny inclusion…this one < 1 cm in diameter) of light-colored minerals in the host rock, which appears orange in this photo, despite looking gray to the naked eye (see the outcrop photo above). The minerals in the bleb look like "salt and pepper", which has no specific meaning but it suggests that the host rock produced these inclusions when heated as the Tertiary granitic melt (liquid rock before crystallizing) invaded. The gray quartz is easily identified (no longer rosy looking due to heat and pressure) and the white could be albite? but the dark minerals would require microscopic examination to identify.
I have to admit that I am writing this post several days after reaching Marshall Pass, where we discovered that I didn't coin that phrase. Someone felt it worth digging a mine to further investigate remineralization along the fault and intrusion zone following Poncha Creek, and they put their money where their mouth was to build this great road we used.
I have one last point to make about our ride to the Continental Divide; the flat meadow at the top suggested to me that this was a cirque, where a mountain glacier formed before pushing along the fault line that now delineates Poncha Creek. These photos show why I think this.
I don’t think it was as thick as those that formed in Yellowstone and at Beartooth Pass, at the north end of Yellowstone Natl park.
This post begins our trip on CO 69 after we left I-25 about 60 miles south of Colorado Springs. We joined the TAT as we entered the Wet Mountains, a granitic batholith that was intruded about 1.5 billion years ago when this part of N. America was colliding with island arcs (e.g., Japan and Asia today). We left the pavement on a gravel road that is typical of granitic terrains because the quartz and Na feldspar (i.e. albite) forms grains that resist chemical weathering. Here is a photo of our journey’s start.
The second photo is the Spanish Peaks, which are Tertiary (66-2.6 mya) intrusions that look like the old granites but are obviously much younger. As we approach our starting point, we drove over some remnants of the Cretaceous and older sediments I mentioned in the previous post. These younger rocks were originally deposited on the eroded surface as the Proterozoic intrusions (i.e. granite) were exposed over hundreds of millions of years. Now these sedimentary rocks have been in-turn eroded to expose (again) the granites. Geologic history is pretty complex in CO! It became obvious that we were climbing on top of a batholith as we reached >9000 feet within a few miles of our starting point.
This is a photo from a pass near the top of the batholith. This photo shows what the outcrops (aka exposures) of this granite look like.
I took some photos without magnification to show the mineral composition of the intrusion. Here is a photo of a hand sample to identify the minerals.
This rock has a mixture of both Na (sodium) and K (potassium) feldspars and quartz, as indicated. It also contains a dark mineral that is not platy and thus is either pyroxene or amphibole (i.e. like pyroxene but with water in the crystal structure). I don’t see any muscovite (a light-colored platy mineral); this assemblage indicates that it crystallized from a melt (the source liquid of the rock) that came from continental crust originally, but the lack of obvious muscovite suggests to me that it was not a highly fractionated (reprocessed) crustal source. I infer this because muscovite is found in rocks containing rare elements like lithium, beryllium, and tantalum, that require multiple rock forming stages to form minerals (they are mined for these elements).
We descended from the top of the batholith to McKenzie Junction (indicated on the map from the Prologue), where we found the host rock (aka country rock) that this granite intruded into ~1.5 billion years ago (bya). The overlying rock has been identified as a metamorphosed volcanic from chemical analysis, but in the field I really couldn’t say if it was basaltic in origin or a shale (both contain similar dark fine-grained minerals). I found really good exposures that showed how the margins of the liquid granite squeezed into the host rock. Here are a couple.
This is a great photo because it shows the banding of light and dark minerals in the metavolcanic host rock separately from the veins of the intrusion. The banding in the host rock occurs because lighter colored minerals like quartz are formed from elements that are squeezed out of the original homogeneous rock under very high temperature and pressure when mountains are formed. Miners look for these veins when searching for gold, silver, and other valuable minerals but they ignore the metamorphic banding, which has been folded during metamorphosis.
This photo shows some of the host metavolcanic rock (from ~1.5 bya) that was not under enough heat and pressure, etc. to form separate layers like the previous photo. Instead, the veins from the granite intrusion are the only banding visible. This photo was taken only less than one mile from the previous, indicating that the conditions (pressure, temperature, chemistry) within the host rock were highly variable when the veins were created.
There are a couple of other points I would like to mention. First, the creek where the last two photos were taken was generally following the NW-SE trend that has been identified as a fundamental weakness in the deep crust of CO, and thus any more recent movement has followed this trend. This is true of the famous mines like Leadville as well; even the Laramide (Tertiary) mountain building that produced the modern Rocky Mts. follows this trend. The second point is that the greater abundance of minerals containing Calcium (Ca) weather from water action easily and the trails along this creek were muddier than those on the eastern side of the Wet Mountains. Calcium doesn’t fit into very many crystal structures well, except for clays, and we know what clay makes…MUD.
One last point as an aside is that we left the Wet Mountains and arrived at Westcliffe CO, looking on the Sangro de Cristo Range to the west. These are also Proterozoic rocks of metamorphic origin, volcanic and sedimentary. We didn’t go there but here is a photo of them; just on the other side of this range is the Great Sand Dunes Natl. Park.
The last photo I have for this post is of some of the Paleozoic sediments that have survived north of Westcliffe. These were exposed in large cliffs as we travelled northward to go around the Sangre de Cristo Mtns.
This prologue introduces a series of posts that will hopefully capture the look and feel of Colorado (hereinafter CO) from the perspective of an off road enthusiast. I am joining some fellow off roaders to traverse CO from east to west along the Trans America Trail (TAT) as modified for four-wheel-drive vehicles. We are picking up the TAT from MacKenzie CO rather from the SE corner of the state because of time constraints but I hope this post will introduce the parts we miss on our trek. Here is a track of our path across the Rockies overlain on a Google Earth image.
Our starting point at MacKenzie CO is indicated by the white square. I did drive along I25 (US87 on the image)east of the Sangre de Cristo Mtns and I will integrate this as best I can in this Prologue. We won’t be missing too much, however, because we will be going through the San Juan Mtns., which are also a major part of the geologic history of CO.
My primary source for the geology of CO is the excellent book by Halka Chronic and Felice Williams, Roadside Geology of Colorado. I will also use general sources that are appropriate. I am relying on geologic maps from the USGS. I will also use the Colorado Geologic Survey’s available data where I can, including maps.
This voyage didn’t start as far east as previous posts because I have moved to Baton Rouge, only about a mile from the Mississippi River. The first part of the journey in time and space is a retread of a previous trip, as I discussed in a previous post. It begins by crossing the Mississippi River and encountering multiple shorelines as sea level has changed in the last 2.5 my. This journey takes us though the Eocene (56-34 my) sediments of NE Texas as we approach Dallas on I20. As I travelled west along I20, the marine sedimentary rocks; which varied between sands, mud, and limestone (deep water); become older, finally reaching early Cretaceous (~120 my) in Fort Worth.
After heading NW before daylight, I crossed over the angular unconformity between the early Cretaceous sediments and mostly Permian (300-250 mya)sedimentary rocks along US 287 between Dallas and Amarillo (shown by the white line in the map below).
Note how the contour of the Cretaceous (140-65 mya) sediments near Dallas (brown color) cuts across the contours of the Permian sediments to the NW, which are shades of blue. This gap between Permian and Cretaceous sediments represents erosion of this area during an interval that includes the Ouachita Orogeny (~318-271 mya) of the Arkansas, Texas, and Oklahoma, the Marathon Uplift of West Texas, and probably the Llano Uplift of Central Texas. The Permian sediments include most lithologies, from sand and shale to evaporates and carbonates. This area was undergoing rapid changes in the shallow water environments during this time, ultimately leading to uplift and erosion.
As I travelled NW from Amarillo, I saw some Tertiary sediments that formed a cap rock, which formed small ledges where recent erosion had cut into this surface. Tertiary basalt flows started capping older sediments near the NM border as I entered a volcanic field that is contemporary with the Rio Grande Rift over the last 70 my.
My route took me across the NE corner of NM and through this volcanic field. There were several cinder cones and many basalt flows capping Paleozoic sedimentary rocks in this area.
This cinder cone was one of several spaced several kilometers apart. These were isolated whereas a much larger volcano only a km or so away had flows originating from near its base.
The basalt creates resistant surfaces and mesas form. The underlying rock is Mesozoic sandstones. These mesas only covered several miles along I25 as I headed north so this is not a giant field but probably an outlier from the much more extensive volcanics to the SW in NM and west in CO.
The subjacent Cretaceous sandstones are thin to massive bedded with cross bedding visible from the highway in road cuts. It also contains coal seams, which were common from this geologic period. These are still mined and train loads were headed south.
I drove north up I25 on top of the Cretaceous Pierre Shale, which forms most of the Great Plains. This mostly mud rock was deposited by the Western Interior Seaway that covered the middle of N. America. Thick sections of the slightly older Niobrara Limestone were visible east of the interstate whereas the Cretaceous sandstone was dominant until Colorado Springs, with granite plutonic rocks forming the back bone of the Spanish Peaks and the Front Range in the north, but that is another post.
This trip is harder than it looked from a geological perspective. Younger rocks like the Eocene Queen City Sand show more details than we can see in Paleozoic rocks like the Hartselle Fm. in N. Alabama. This makes it difficult to make sweeping statements about them. Anyone who has visited the central Gulf of Mexico knows it looks muddy, but the sand lies at the bottom and wherever the waves are strong enough to remove the finer clays. The ledges of Barwnmell Mtn. are mostly mud as described in the previous post, but there is no clear separation of mud from sand in a delta, where enormous amounts of mixed particles arrive from rivers like the Mississippi River. This photo was taken with a 15x macro lens on my iPhone. It shows sand grains in the shale sample I discussed before.
Most of the shiny particles are sand grains. This is important from a wheeling perspective, because even a little sand in a fine matrix improves traction (like the paint we buy for porches and garages). Both of the samples I collected contained these sand grains.
The next major issue I discerned from my samples and trip was the red mud, which is the result of oxidation of iron (Fe) with lots of oxygen. The samples were both dark grey inside, which indicates no iron oxidation The red color seen in concentric zones in my samples, and the entire mountain, was from exposure of these sandy shales to the atmosphere as they erode and fracture. This photo with the 15x lens shows the amount of void space (i.e. porosity) in these rocks.
Note the small pores seen in this image, which fill with water in this part of Texas, but with oil far to the south. I can’t explain easily the blue color, which was not seen until the magnification was this great.
This brings me to the last (almost) point I want to take from this trip. The sedimentary rocks deposited in the SE U.S. (specifically AL and TX) contain a large amount of iron, which produces iron ore (e.g. Birmingham was the only major iron production center in the south prior to the U.S. civil war). These rocks also contain so much Fe that they must be filtered for consumption from water wells in NE TX. Geologists don’t know why because the source rocks for all of this Fe are long gone (they’re remnants reside in these rocks and the Black Warrior Basin of AL). Iron has been mined from carbonates (limestone) in PA from this geological period, but that is another story. The bottom line is that when ocean (aka marginal sea) circulation is just right, there is not enough oxygen to keep Fe active (so to speak). This is very localized, which brings me to my final point.
This photo from Wikipedia says it all. Just look at all of those thin strands of land and the isolated bodies of water that separate them…
Enough said about my limited understanding of NE TX geology, but it does make for interesting wheeling…next stop, Colorado…see you there and then!
This post isn’t about somebody overturning (I don’t think anyone did), but the reversal of expected geology in mixed sand/mud environments. I start by referring to the wheeling experience at Hawk Pride, where we fought mud that was produced from weathering (erosion) of shale and sandstones. There, we found boulders of Hartselle Fm. sandstone in a hillside with lots of shale/mud, where the ledges (an offroad term for a hard climb over a solid layer of rock) were the more resistant sandstone. BUT, those were 300 my old sediments where the quartz grains produced a silica cement, which made the “sandy” layers really hard.
As I mentioned in a previous post, these rocks are only 50 my old, and the sandstone is not cemented, which is why the layers (in total) are called the “Queen City Sand”. Here is a (poor) image that shows what I mean…
The vehicle in the image was dragged (by winch) over a 2 foot ledge of hard rock, which can be inferred from their exit (sorry about the poor trail photos, but I forget to take them when I am worried about my own escape…a work in progress). The ledge was composed of shales like I showed in the previous post. Here is another photo of a hand sample from this area. The rock doesn’t have as many organic components but it is as resistant.
This post is difficult to write because I didn’t take enough photos of the trail geology, but it is important to learn one lesson…time heals all sedimentary wounds…the young Eocene rocks (~50 mya) haven’t had time to heal all wounds. I mean that the organic material was still observable in a hand sample, and the sands didn’t supply silica (aka SiO2) to cement them as with older rocks. The result is that we were attempting to drive over hard shale (aka mud) layers while the sand formed nice traction surfaces to approach these ledges.
I will try and tie the environmental, geological, and wheeling aspects of this trip together in the next post, the epilogue…
Barnwell Mountain consists of one geologic formation, the Queen City Sand. As suggested by the linked report, and others related to water wells in the NE TX area, this formation comprises unlithified (not cemented) sandy layers and muddy layers that are somewhat more resistant to erosion. This formation has been described (reference unknown but government agency source) as a primarily sandy unit that was deposited in a constructive coastal environment (i.e. more sediment than could be transported away) that was part of a lobate delta system, including delta plain, delta front, and prodelta facies (i.e. sedimentary depositional environments). This is a concise description of the Mississippi River delta today, with numerous inactive deltas, lots of sediment (especially mud), and a wave-dominated sandy barrier island system where the river finally must deal with the ocean head-on…
I took a nice photo of an outcrop within the geology compass Ap but it cannot apparently be downloaded…here is a photo (actually more useful) of the blocks of nodular, fossiliferous, dark grey mudstones that formed ledges (<2 feet high) and erosional blocks within the park.
It is a quirk of younger rocks that the sandy layers are difficult to cement because of the great pressure and temperature necessary to recrystallize quartz into a silica cement (microcrystalline), whereas mud can be lithified more easily because of all of the organic contaminants found in fine-grained sediments in coastal environments. The result of this is that there is a lot of sand found all over the mountain, but no obvious source because the mountain is made of sand (maybe some weak cement but not silica). Here is a photo of a sample I procured from the campsite, which is representative of other layers in the park.
Note the nodular surface that almost looks like walnuts. This is another example of how bedding layers, like the surface of this sample, are produced by chemical and not physical processes (enough about that!). When I broke this open, it almost looks like some mud from the slough behind my house…
This photo shows the walnut/nodular surface and inside one of these nodules. We see concentric layers based on slight chemical differences in the original mud, and some darker, partly recrystallized, dark matter that is probably a piece of wood (very resistant to recrystallization,,,I think?) or other crap…geologists must use very expensive methods like electron microscopy to identify these kinds of substances. The gaps in the pore space are obvious…these would be filled with water, gas, or (Texans hope) OIL. The next photo shows how much these Eocene (~55 mya) sedimentary rocks resemble modern sediments (a Hoorah for Uniformitarianism)…
This sample is difficult to describe…it contains a lot of “stuff” that is apparently biological in origin, a lot like the muck I dig out of the slough behind my house. Some of the material even has a lighter color, suggesting it is quite different mineralogy or even original material, but I have no idea about this without more thorough study of the sample. I will close this post with the thought that mud is mud is shale is mud, ad-nauseam!
As noted in the prologue post, we moved back in time as we travel northeast, just as in driving to NE Alabama. The difference between these two drives is the time-interval covered by our 8-hour drive; we time-traveled 330 my (million years) to go to AL whereas the trip to TX only covered about 60 my.
The ancestral Appalachian Mtns. were located all along the eastern seaboard as they still are today. All of those rocks and the titanic collision with Africa pushed the earth’s crust downward as well as upward, as vast quantities of sediment were eroded from the rapidly rising mountains. Thus, the Mississippian Era (~330 mya) rocks deposited in NE AL were buried deep (and produced oil and coal because of it), but the crust has rebounded over the last several HUNDRED million years and these old, previously deeply buried sediments from a delta are now exposed at Hawk Pride ORV park.
When I drove to Gilmer, instead of seeing a regular, albeit incomplete (due to erosion) stack of sediments, I drove over Pleistocene (<2 mya) terraces produced by changes in sea level on a relatively stable coastline. There were also missing rocks as in Mississippi, especially the gap between the Pleistocene terraces (~2 mya) and the Miocene rocks we encountered near Natchitoches (~20 mya), and the even longer diastem (missing rocks) between the Miocene and Eocene sediments we will see in Gilmer (~40 mya). As we get into older sediments, they become more uniform (i.e. the smooth transition from Eocene to Paleocene near the TX-LA border on I-20.
This post is intended to remind me of the similarity of the rocks and history on the east and west sides of the MS embayment, which has little to do with the ancestral Appalachians but it does overprint its impacts on the older ones…We must always think 4-dimensionally with geology…LOL