The table of contents may be found here.
A modern erg, similar to those that dominated the Jemez area in the Mesozoic.. NARA
The Mesozoic was the Age of the Dinosaurs. Its beginning and end
were bookended by mass extinctions, in which a large
fraction of the families of fossils disappeared in a geological
blink of an eye. Life took millions of years to recover its
In this chapter, we will look at the Jemez area during the Mesozoic Era
The oldest Permian formations in the Jemez area are separated
from the youngest Triassic formations by a significant
unconformity. As a result, there is no direct record in the Jemez
of one of the greatest catastrophes in the history of the Earth.
Starting about 252 million years ago, some 96% of marine species
and 70% of land species went extinct in a geologically brief
period of time, a dramatic enough change in the fossil record that
it was chosen by geologists to mark the boundary between the
Paleozoic Era and the Mesozoic Era. It took around ten million
years for the diversity of life to recover.
Geologists are still debating just what went wrong. There is evidence that global temperatures abruptly rose, by 8C (14F), accompanied by a sharp increase in atmospheric carbon dioxide levels, to over seven times its modern preindustrial value. There is also evidence of a surge in the ratio of biologically active carbon-12 to less biologically active carbon-13. This suggests a massive release of biological carbon into the atmosphere, which could have been caused by a global fire storm or some other massive destruction of vegetation. There is weaker evidence of repeated explosions of the fungus population, and it has been suggested that the fungus were fed by large quantities of dead vegetation. There is also evidence of an increased mutation rate in plant spores, which some geologists interpret as evidence of increased ultraviolet light reaching the Earth's surface.
The exact timing of this extinction is hotly debated, with some geologists pointing to evidence of a single massive extinction pulse and others pointing to repeated pulses of extinction over a period of up to 10 million years. Part of the difficulty is that the gap in the geologic record in the Jemez at this time is not at all unusual. Sea levels were nearly as low as at any time in the geologic record, reducing opportunities for sediments to accumulate. There are few places on Earth where the rock beds span the Permian-Triassic boundary, which is one reason why there is uncertainty just what took place. However, the geologic record for this time is reasonably complete in Sichuan province, China, and very precise dating of zircon grains in ash beds suggests the extinction took place between 251.941 ± 0.037 and 251.880 ± 0.031 million years ago.
Among the candidate causes is an asteroid impact like the one
widely believed to have caused the extinction of most dinosaurs.
However, the crater from this impact has not been positively
identified. It may never be identified; an asteroid is twice as
likely to hit the oceans as the continents, given the relative
areas, and the oceanic crust is recycled in less than 250 million
years. So a crater on the ocean floor from 250 million years ago
would be long erased. Some candidate craters on land have been
identified, but it is not clear that the proposed candidates are
actually impact craters or that they are large enough to account
for the extinction.
Another possibility is that the extinction was caused by the eruption of the Siberian Traps. These are colossal lava flows, covering an area of northern Siberia the size of western Europe, that were erupted pretty much at exactly the right time. This huge eruption may have been caused by a asteroid impact, either at the eruption location or exactly opposite it on the Earth's surface; computer models show that the shock from a major impact converges at the opposite side of the Earth and could cause significant disturbance of the crust and upper mantle. There is even some evidence of an impact crater, the Wilkes Land Crater in Antarctica, which would have been opposite Siberia at the time.
Perhaps neither an impact event nor the Siberian Traps eruption
alone caused the "Great Dying." The Siberian Traps erupted through
rock rich in coal and carbonate, and would have released large
amounts of carbon dioxide. This could have had lasting effects on
the climate, as could an explosion in the population of
methane-generating bacteria proposed by other geologists. The
near-record low sea levels meant fewer shallow marine
environments, magnifying the effects of global stress on marine
families of life
The Triassic opened with Pangaea fully assembled. A large
island arc collided with southwest North America sometime in the
late Permian or early Triassic, producing the Sonoma Orogeny. Up
to 300 km (200 miles) of crust was sutured onto the west coast.
The force of the collision produced great thrust sheets,
layers of rock driven eastward many kilometers over the existing
crust. Though these sheets did not reach as far east as the Jemez
area, the disturbance elevated the region enough to bring it well
above sea level and produce a major unconformity on the
Later in the Triassic, Africa began to split away from eastern North America, and vast red bed deposits were laid down in the Appalachian area. The Gulf of Mexico began to open late in the Triassic. The breakup of Pangaea would continue for another 150 million years.
Conifers became the dominant form of land vegetation, and the first true mammals emerged late in the Triassic from a group of mammal-like tetrapods called therapsids.
We pick up our story in lower Cañon de San Diego, where the upper
Permian and lower Triassic columns are well displayed in the sides
of Meseta Blanca.
Meseta Blanca. Looking north from 35 39.979N 106 42.869W
At the bottom are the red beds of the Permian San Ysidro Formation, Yeso Group. Above these are lighter beds of the Glorieta Formation. Then comes a discontinuity and the gentler slope and darker beds of the Triassic Moenkopi Formation, and finally the steep slope and lighter beds of the Shinarump Formation, with a cap of dark ferruginous conglomerate.
Relief map of the Jemez with Moenkipi Formation outcroppings highlighted in red.
The Moenkopi Formation is the oldest Triassic formation in the
Jemez area. It is composed of thin beds of dark brown mudstone and
sandstone and tends to form slopes between cliffs of the harder
sandstones of the underlying Glorieta Formation and the overlying
Shinarump Formation. It is separated from both by unconformities.
Moenkopi Formation. 35 39.987N 106 42.866W
Moenkopi Formation. 35 39.975N 106 42.877'W
Under the loupe, the sample here is revealed as a poorly sorted coarse sandstone of well-rounded quartz and lithic grains with abundant cement filling the pore spaces -- probably enough that the rock is matrix-supported rather than clast-supported: A lithic wacke.
The Moenkopi was laid down around 240 million years ago, at a
time when the Appalachians were a mighty mountain chain and great
rivers flowed west from their foothills towards the Pacific. The
area from the Jemez across what is now the Colorado Plateau was
very flat and arid, and only the largest rivers made it clear to
the ocean. The shifting rivers laid down the mudstone of the
Moenkopi in what was likely a tidal flat environment. The Moenkopi
beds are relatively thin in the Jemez, but are up to 300m (1000')
thick in parts of southern Utah. Particularly good exposures are
visible in the Hite
Moenkopi and Shinarump Formations. 35 39.851N 106 42.844W
This transition is visible even on the satellite view of Google Maps. This contact can be mapped throughout the Colorado Plateau, and marked a brief period of lowered sea levels and erosion. The entire Jemez area was high ground at this time.
Perhaps the most spectacular exposure of the Permian and Triassic rock column in the southwest Jemez is on the western slopes of Guadelupita Mesa southeast of Guadelupe Box.
Permian red beds on the west side of Guadelupita Mesa. Looking southeast from 35 43.982N 106 45.840W
At right, at the base of the mesa, there are thin beds of the Abo
Formation. Above these are massive beds of the Meseta Blanca
Formation, Yeso Group. To the left, a fault has thrown the Meseta
Blanca Formation down by a good hundred feet or so, and thin beds
of San Ysidro Formation, Yeso Group, are visible above. Then comes
a thin lighter layer of Glorietta Sandstone, then more red beds of
the Moenkopi Formation, topped by Shinarump Formation and much
younger Bandelier Tuff.
The Moenkopi Formation here and to the north was originally
mapped as Bernal Formation. In the Glorietta area, where the
Glorietta Formation was first described, the Bernal Formation is a
mudstone formation overlying the Glorietta Formation, and it
resembles the Moenkopi Formation enough for the two to be easily
confused. It took some time for geologists to correctly identify
the muddy beds immediately above the Glorietta Formation in the
Jemez. However, the Bernal Formation is a late Permian formation,
while the Moenkopi Formation is a middle Triassic formation.
Ironically, the Bernal Formation beds of Glorietta Pass are now
assigned to the Artesia Formation.
Relief map of the Jemez with Chinle Group outcroppings highlighted in red.
230 million years ago, northern New Mexico was part of a broad
river plain located between the eroded remnants of the Umcompahgre
Highlands to the north and the Mogollon volcanic arc well to the
south, in what is now southern Arizona and northern Mexico. A wet
season of drenching rain alternated with a long dry season to
produce a monsoon climate, typical of continental regions just
north of the tropical rain belt. The mighty Chinle River,
comparable to the modern Mississippi River, meandered westward
from the young Appalachians and passed very close to the Jemez
area before draining into a shallow sea somewhere in western
The rivers and lakes supported stands of cycads, horsetails, and
primitive conifers, which in turn supported a population of large
amphibians and early dinosaurs. These included Coelophysis,
now the New Mexico state fossil.
The Triassic formations of the Jemez area younger than the Moenkopi Formation are assigned to the Chinle Group. These rocks are thought to have been deposited by the Chinle River. Zircons have been identified in Chinle beds that show chemical signatures identical to granites exposed in the southern Appalachians today. The river system was long-lived and deposited vast quantities of sediments in its valley and delta.
The formations of the Chinle Group vary considerably across the Jemez. The lower formations in the northern Jemez are visible in the road cut west of Canones.
Lower Chinle Group. 36.2356743N 106.3960087W
The dark muddy beds at bottom are the uppermost beds of the
Arroyo del Agua Formation of the Permian Cutler Group. The comes
an unconformity and the massive pinkish sandstone beds of the
Shinarump Formation, around 230 million years old. Then comes a
thin mudstone layer of the Salitral Formation and, at the top of
the road cut, conglomerate and sandstone of the Poleo Formation.
In 1872, Congress authorized a survey to map the United States
west of the 100th meridian on the scale of eight miles to the
inch. The Wheeler Survey focused on the southwestern United
States, and in 1873 it produced some of the first good topographic
maps of New Mexico. With the Survey was G.K.Gilbert, who assigned
some of the first formation names to beds exposed on the Colorado
Plateau. Among these was a sandstone and pebble conglomerate of
Triassic age, which he named the Shinarump Conglomerate in 1875.
In 1957, John H. Stewart reassigned these beds to the Shinarump
Member of the Chinle Formation. The Chinle Formation was
controversially promoted to group status by Lucas in 1993, and New
Mexico geologists accordingly tend to speak of the Shinarump
Conglomerate as a formation in its own right.
Relief map of the Jemez with Shinarump Formation outcroppings highlighted in red.
In the Jemez region, the Shinarump Formation is the lowest
formation of of the Chinle Group, and it fills valleys and other
low spots cut into the Moenkopi Formation. In the southern Jemez,
it takes the form of massive sandstone beds with lenses of
conglomerate, produced by early erosion off the newly raised
Mogollon highlands. Because the Shinarump Formation is highly
resistant, and is overlain by much more poorly cemented sediments,
it often caps mesas, as at Meseta Blanca.
Shinarump Formation. 35 39.844N 106 42.814W
A sample of a conglomerate lens:
Shinarump Formation conglomerate. 35 39.844N 106 42.814W
Under the loupe, this is seen to be a moderately well-sorted fine
conglomerate of well-rounded quartzite pebbles cemented together
with abundant tan matrix. A sample of the sandstone:
Shinarump Formation sandstone. 35 39.844N 106 42.814W
The sandstone is a well-sorted, coarse sandstone composed of
angular quartz grains with a modest amount of cement.
One of the most extensive exposures caps a downwarped plateau at the southern end of the Sierra Nacimiento. The downwarp is mapped as Jack Rabbit Flats, while the escarpments bounding the plateau to east and west form Mesa Chuchilla and Red Mesa, respectively. Red Mesa displays an impressive Permian rock column capped with Moenkopi Formation and Shinarump Formation.
Red Mesa. Looking east from 35 35.830N 106 53.489W
The near terrain is red beds of the Triassic Petrified Forest
Formation, which we will come to shortly. These younger beds are
thrown down many hundred feet by the Pajarito Fault, which lies at
the base of Red Mesa.
Further north, the Moenkopi is not present, and the Shinarump Formation sits directly on Permian red beds. The Shinarump continues to be a prominent formation in the western Jemez, where it caps a number of mesas. These include Eureka Mesa.
Eureka Mesa. 35
59.409N 106 52.648W
Underneath are beds of the Permian Yeso and Abo Formations.
Further north, the Yeso Group thins and disappears, and the
Shinarump sits directly on Cutler Group beds.
Older papers and maps, such as Wood and Northrop's 1946 map,
identify the Shinarump as the Agua Zarca Sandstone Member of the
Chinle Formation in the western Jemez. Some more recent writings
attempt to reconcile terminology by designating these thick
sandstone beds as the Agua Zarca Member of the Shinarump
The west end of Eureka Mesa is the location of the Nacimiento Mine, where the Shinarump Formation was once mined for copper ore.
Nacimiento Mine showing Shinarump
Formation beds. 35
59.543N 106 54.077W
Here the Shinarump beds begin to dip steeply into the Nacimiento
Fault, located just west of the mine. The Shinarump forms the
light beds to the left and the partially excavated beds and large
boulders near the center of the panorama. The underlying Yeso and
Abo beds are exposed in the reddish area directly across the lake,
while the younger Triassic Salitral Formation forms the reddish
beds at extreme left and right.
The Shinarump is locally rich in petrified wood.
In some locations, the wood has been replaced by copper minerals
such as chalcocite, Cu2S, rather than the usual silica.
The chalcocite is mined as copper ore.
The Salitral also shows local concretions.
These are localized deposits of particularly large quantities of cement in the sandstone. We will see many further examples in this chapter.
These may be flute casts.
Flute casts are a form of sole mark, formed by water flowing over the surface of a mud bed and eroding channels in the mud. These are later filled in with sand or silt. If the marks here are in fact flute casts, then the face of the boulder was once at the bottom of the bed and the flow was towards what is now the bottom of the boulder. However, the boulder has obviously been disturbed (it is part of the landslide area) so it’s not possible to reconstruct the original orientation and flow direction from this example.
Some of the conglomerate in the Shinarump is very coarse.
This may be from the axis of a river channel, and the associated
petrified wood may be a fossil log jam in the river,
possibly at one end of a point bar.
Aerial photograph of river with point bars. U.S. Geological Survey
A point bar is an accumulation of sediments on the inner
downstream side of a meander in the river. Point bars tend to
accumulate organic debris as well.
The unconformity dividing the Permian from the Triassic is
beautifully exposed In the Canones
fault zone along the western boundary of the Rio Grande
Rift. We visited this area in the last chapter, but it's time to
Permian and Triassic sedimentary beds. As with all photos here, click to enlarge. 36 14.033N 106 23.336W
The lowermost red rocks, with the many layers and the column-like
structures, belong to the Arroyo del Agua Formation of the Cutler
Group. We examined this in the last chapter. The massive bed above
the Arroyo del Agua Formation is the Shinarump Formation.
Here is the contact between the Arroyo del Agua and the Shinarump close up:
The lower part of the Shinarump Formation is a thick bed of
This stands out clearly in the outcrop photographs earlier. The
sandstone is a well-sorted coarse quartz arenite. Somewhat to my
surprise, there is little or no calcite, the cement apparently
being additional silica.
Just above the thick sandstone is an impressive bed of
The clasts resemble those in the Shinarump conglomerate beds south of the Jemez, but there is much less tan matrix between the clasts.
The Shinarump Formation can be traced into northwest Arizona, but
it thins to the north, although it can still be mapped in
Canyonlands National Park.
Conglomerate is a clastic sedimentary rock containing a
substantial number of clasts that are larger than 2mm in diameter.
Thus the coarsest sandstones grade into fine conglomerate. At the
other end of the size scale, conglomerates may be dominated by
clasts the size of boulders, and we'll see some striking examples
later in this book. The spaces between the large clasts are almost
always filled with a matrix of finer sediments, such as
sand or clay. A well-consolidated, highly indurated
conglomerate resembles nothing so much as a slab of concrete, and
concrete may be thought of as artificial conglomerate.
If the matrix is scanty enough that the clasts touch each other,
the conglomerate is described as clast-supported, because
the clasts take up the weight of the overlying rock. If the matrix
is more abundant, so that it actually separates the clasts, the
conglomerate is spoken of as matrix-supported. As with
sandstones, a conglomerate can be well-sorted (with clasts
mostly the same size) or poorly sorted (containing a
jumble of clasts of various sizes), though well-sorted
conglomerates are not common. Manufactured concrete is strongest
when it has just enough sand and Portland cement in the mix to
correspond with a conglomerate that has abundant matrix but is
still clast-supported. (Manufactured concretes also tend to be
Geologists distinguish conglomerates having rounded, polished
clasts from breccias, which have angular, broken clasts.
Conglomerates are typical of a very high-energy environment, such
as a fast-running river bed, where very large rocks are tumbled
and polished. This is rarely found far from the source outcrop.
Breccias are almost always found very close to their source rock,
since they have not been transported far enough even to round and
polish the clasts. They tend to form from catastrophic events,
such as landslides, earthquakes, meteor impacts, or volcanic
The large clasts in a conglomerate can easily be examined to determine their rock type and thus identify their source. In young conglomerates, the source rock may be an obvious nearby outcropping or highland. In ancient conglomerates, the source rock may long have eroded away or been buried, and the conglomerate then provides the best information we have on the rock composition of an ancient uplift.
The Shinarump conglomerate sample shown above is a moderately well-sorted clast-supported conglomerate composed of bits of quartzite that weathered from the flanking uplifts of the Ancestral Rocky Mountains.
Below is a paleogeologic map of the surface on which the
Shinarump was deposited.
Paleogeologic map of the lower Shinarump Formation surface in the Jermez.region
This map shows the age of the formations immediately under the
Shinarump. Green shows areas where the Shinarump lies on the
Moenkopi Formation, the next youngest formation in the Jemez. Red
is the Yeso Formation, and yellow is the Abo Formation or Cutler
Group. This map shows that the younger formations are present
under the Shinarump to the south and east while the older
formations are present to the north, with the oldest formations of
all (Abo and Cutler Group) present directly north and to the
northwest of the Jemez.
The interpretation is a bit ambiguous, since this does not tell
us whether the missing beds were ever laid down or exactly when
they were eroded away if they were once present. One might suppose
that the yellow areas mark significant areas of uplifted ground
associated with the ancestral Rocky Mountains. Evidence from the
surrounding region, including paleocurrent analysis (in
which sedimentary structures are studied for evidence of ancient
river courses), suggests that the Sierra Nacimiento was indeed a
region of uplift but the area immediately north of the Jemez was
not. Instead, this area likely marks the early course of the
Chinle River, which, when still young, was likely a powerful agent
Relief map of the Jemez with Salitral Formation outcroppings highlighted in red.
The greatest thicknesses of the Salitral Formation in the Jemez occurs to the northwest, where it takes the form of red to brown mudstone. We've seen a photograph of the Nacimiento Mine that shows Salitral Formation atop the Shinarump and along the south side of the lake filling the former open pit mine. The Salitral here is notable for septarian nodules, formed when mud concretions in the beds dry and crack internally. The cracks are later mineralized by groundwater.
This photograph shows a septarian nodule from the Nacimiento Mine
that has been cut in half and polished.
The white crystalline filling is made of calcite. This glows a
beautiful blood red when exposed to ultraviolet light, like all
but the purest calcite. The color likely comes from traces of
manganese replacing calcium ions in the calcite. Manganese is a
moderately abundant element whose ions typically have the same
charge (+2) and roughly the same radius as calcium ions. However,
manganese is a transition metal, with unpaired electrons in its
inner shells that scatter and absorb both visible and ultraviolet
light. This gives many manganese compounds bright colors and
allows traces of manganese to fluoresce under ultraviolet light.
The Salitral Formation is a very weak shale where it crops out
just above the Shinarump Formation at the Nacimiento Mine.
In the southern Jemez, the upper beds of the Shinarump Formation transition into a very coarse ferruginous conglomerate. The geologic map notes that these ferruginous beds are suggestive of the dark mudstones of the Salitral Formation, though this formation is not mapped in the southern Jemez.
A ferruginous sedimentary rock is one containing large quantities
of iron oxides. These give the rock a dark color and a high
density. Like the ferruginous Log Springs Formation further west,
these beds probably formed from prolonged leaching of soil in a
The Shinarump and Salitral Formations are thought to represent development of river deltas along the Chinle River, with the sandstone and conglomerate of the Shinarump being deposited first and the mudstone of the Salitral later as the river valley filled and the river slowed.
Relief map of the Jemez with Poleo Formation outcroppings highlighted in red.
Above the Shinarump and Salitral is the Poleo Formation, which is
very prominent north of the Jemez.
The Poleo Formation tends to cap mesas, since it is very
resistant to erosion. It forms the rim of the road cut in the
Canones Fault Zone that we have visited before. A strand of the
Canones Fault is found just
west of the main fault and puts the bottom of the Poleo
Formation to the east against the middle of the Poleo Formation to
In a few places along this road cut, the Poleo Sandstone overhangs enough to provide a nice nesting spot for swallows.
These are likely nests of Petrochelidon pyrrhonota, the
American cliff swallow.
A little further down the highway, there is a turnoff to a gravel
road leading to a bench of Poleo Sandstone along the Chama River.
Here's a sample of the sandstone from this area.
Poleo Sandstone from 36 13.965N 106 23.871W
It's a very clean sandstone composed of nearly pure quartz. The grains are fine, well-rounded, and well-sorted. This is an excellent example of a supermature quartz arenite.
The mature sandstone of the Poleo Formation tells us that the
climate in the Jemez area became arid enough for windblown dunes
The view south from this bench takes in rocks of very different ages.
At the left, the Rio Chama winds around a mesa capped with Poleo
Sandstone. The reddish area in the drainage to the south is an
outcrop of the Painted Desert Member of the Petrified Forest
Formation of the Chinle Group, which sits atop the Poleo
Formation. To the right is more Poleo Formation. There is a strand
of the Canones Fault on the west (right) side of the drainage that
has dropped the Petrified Forest Formation down on the east.
The mesa on the skyline is Canones Mesa.
The zone of faulting and deformation along the southeast margin of the Colorado Plateau has been traced as far west as Coyote.
At Abiquiu Dam, the Poleo Sandstone is particularly thick.
The Poleo Formation grades into the overlying Painted Desert Member, without a very sharp transition. We see this just south of the dam, where the sandstone beds of the Poleo Formation begin to be interbedded with red mudstone.
Crossbedding is particularly prominent in a road cut along a maintenance road east of the main highway.
East of Abiquiu Dam. 36 14.427N 106 25.691W
The vertical structures are drill holes where engineers blasted
out the road bed.
Still further west, the Poleo Formation underlies La Joya del Pedregal ("Jewel of the Stony Ground":
La Joya del Pedregal. 36 13.477N 106 30.703W
The flat plain here is likely not an erosional surface, but a surface underlain by the resistant Poleo Formation. Basalt clasts from the Jemez volcanic field to the south accounts for the “stony ground”; “jewel” is a conceit.
At left is Cerro Pedernal, one of the most prominent landforms of the nothern Jemez, and a favorite subject for the paintings of artist Georgia O'Keefe. We'll learn more about this relatively young feature several chapters on.
The Poleo Sandstone is also prominent on the mesas west of Coyote, but begins to thin to the south. It is just a few meters thick at the Nacimiento Mine west of Cuba, where it is also strikingly thinly bedded.
Poleo Sandstone at Nacimiento Mine. 35
59.499N 106 53.988W
The Poleo Formation becomes spotty in the southwest Jemez, where the Salitral Formation pinches out and the Poleo becomes difficult to distinguish from the uppermost beds of the Shinarump Formation.
Relief map of the Jemez with upper Chinle Group outcroppings highlighted in red.
As the Chlnle River matured and become a mighty river, comparable with today's Mississippi River, it carried increasing quantities of fine sediments. These were supplemented with ash from the volcanoes of the Mogollon Highlands to the south, which quickly weathered into red clay. This was deposited as the Petrified Forest Formation, sometimes mapped in the Jemez simply as the upper Chinle Group. Silica from the volcanic ash replaced organic matter in logs buried in the sediments to form petrified wood, which is most abundant in eastern Arizona in the Petrified Forest. However, the formation is prominent as far east as the Jemez.
Like the Shinarup and Salitral Formations, the Poleo and Painted
Desert Formations are thought to represent the growth of a river
delta through the area. All these Triassic formations are assigned
to the Chinle Group. At this time, much of western North
America was covered with flood plains and swamps.
In some locations, there is a thin bed of the Mesa Montosa Member of the Petrified Forest Formation atop the Poleo Formation.. The highway cuts through such a bed here.
In this location, at least, the Mesa Montosa Member is much better consolidated than the overlying Painted Desert Member. There are numerous veins lined with calcite crystals through this bed. I picked up a particularly pretty example.
The bulk of the Petrified Forest Formation north of the Jemez is
assigned to the Painted Desert Member. This is found above the
Mesa Montosa Member where the latter is present, or else sits
directly on the Poleo Sandstone.
The Painted Desert Member is a distinctive red from all the hematite it contains. It is almost nowhere very well cemented. The outcropping here is basically red dirt, and my sample has already almost crumbled away:
Under the loupe, the grains look very much like those in the
Poleo Sandstone, but the pore space is much more open, and the
rock is obviously much less thoroughly cemented. There are also
more feldspar grains in among the quartz, though not enough to
make this an arkose.
West of Abiquiu Dam, there is a road cut through a thick and spectacular section of the Painted Desert Member.
Painted Desert Member in roadcut south of Abiquiu Dam. 36 14.046N 106 25.824W
The formation is easily eroded to form a gullied surface. The
gray-green layers are most likely beds unusually rich in organic
matter, so that the red ferric iron was reduced and leached away
to leave whitish clay.
Here is a close up view of the formation, showing that it is a thinly bedded red shale that easily weathers into red mud.
Painted Desert Member in roadcut south of Abiquiu Dam. Quarter for scale. 36 14.046N 106 25.824W
Mudstone is actually more typical of the Painted Desert Member
than the dirty sandstone shown earlier, which may be transitional
with the underlying Mesa Montosa Member.
The road curves around south of the reservoir and at a pullout one has a nice view of the Abiquiu Reservoir.
In the distance are cliffs of Mesozoic rocks of the Colorado Plateau. In the middle distance is the reservoir, whose shores are mostly Poleo Formation under rounded hills of Painted Desert Member. In the foreground, dark boulders are Lobato Formation basalt. The Painted Desert Member and other formations underlying the Lobato Mesa Formation basalt flows to the south lack strength, and this makes for landslides. A large landslide appears to cover the entire area immediately south and east of this point.
So the rock column in the northern Jemez for the Mesozoic that
we've seen so far is: Permian Arroyo del Agua Formation, Cutler
Group; Shinarump Formation, Chinle Group; Poleo Sandstone, Chinle
Group; Mesa Montosa Member, Petrified Forest Formation, Chinle
Group; and Painted Desert Member, Petrified Forest Formation,
of Youngsville one sees the same sequence of beds exposed,
at Mesa Naranja.
The lower red portion of Mesa Naranja is Arroyo del Agua Formation, and the thin white band near the top is the Shinarump Formation. Above this is soft shale of the Salitral Formation on which rest fractured beds of the Poleo Formation. This is the same sequence we saw back at the Canones road cut, but here the Salitral is much thicker.
In the southern Jemez, the upper Chinle beds are all assigned to the Petrified Forest Formation. This is especially well exposed along White Mesa.
The uppermost beds of the Chinle Formation north of the Jemez
were long described simply as the upper siltstone member. With the
promotion of the Chinle Formation to group status, these beds were
reassigned to the Rock Point Formation. The Rock Point
Formation is exposed in a few locations in the northern Jemez,
including near the entrance to "Mushroom
Canyon" along Forest Road 100 south of Youngsville.
Here the contact between the Rock Point Formation and the Jurassic
Entrada Sandstone is exposed in the canyon wall.
The Rock Point Formation is the uppermost formation in the
Triassic Chinle Group in the northern Jemez, aged about 205
million years. The overlying Jurassic Entrada Sandstone has an age
of about 160 million years. The intervening 45 million years are
missing from the geological record here.
The Rock Point Formation is fairly hard siltstone
Exposures of the Rock Point Formation near Ghost
Ranch have yielded hundreds of fossilized skeletons of Coelophysis,
the oldest dinosaur for which complete skeletons have been
recovered in North America.The most important dinosaur quarry in
this area is the Whitaker quarry, discovered in 1948. Other fossil
quarries are found at Canjilon, Hayden, and, most recently, the
rich Snyder quarry, discovered in 1998. The Snyder quarry has
abundant carbonized wood, suggesting the fossils there were from a
mass death attributable to a forest fire, some 210 million years
The Chinle Group disappears to the south under the volcanic rocks of the Jemez Mountains, but reappears south of the Valles caldera in the Valle de los Indios and in the area around Ponderosa. The geological column from Permian to nearly the present day is displayed on the south wall of the Valle de los Indios as seen from its the north rim, a location reached by a short hike from Jemez Falls Campground:
In the foreground, close to the camera, are outcrops of very young South Mountain Rhyolite. We'll revisit this again towards the end of this book. This is also visible in the cliffs to the left across the canyon. Here we see part of the south rim of the Valles Caldera. The prominent red to white cliffs in the lower half of the canyon wall are probably Permian Glorietta Sandstone, although there are outcrops of brighter orange Yeso Group sandstones just visible under the Glorietta Sandstone right of center. The heavily forested middle slopes, above the sandstone cliffs, are Moenkopi Formation and Chinle Group beds. These are very poorly exposed in this location. The prominent white cliff at top center is Otowi Member, Bandelier Tuff.
Still further south, near Paliza
Canyon Campground, the Petrified Forest Formation underlies
Bandelier Tuff on the north side of the canyon.
This poorly consolidated formation underlies much of the
Ponderosa area. It also found below younger formations on the west
face of Borrego
Mesa, and here there are very
large landslide deposits where the mudstone has given way
from under the lava flows capping the mesa. Chinle mudstones are
exposed in some of the landslide scarps along the face of
Painted Desert Formation exposed in landslide scarp. 35 40.571N 106 38.48W
A landslide scarp is a portion of an unstable slope left behind
when the lower part of the slope breaks loose and slides
downslope. The scarp is typically cliff-like and concave, as you
see in this photograph.
Just north of Ponderosa there are impressive outcroppings of the Agua Zarca Sandstone of the Shinarump Formation, Chinle Group, exposed west of the road.
Agua Zarca Sandstone, Shinarump Formation. 35 40.225N 106 39.774W
Under the loupe, this rock appears almost identical with the
Poleo Sandstone north of the Jemez.
Across the road is a knob
topped with what my road log identifies as Poleo Sandstone.
If this has been correctly identified, then the red mudstone
beneath is Salitral Formation.
Consider the differences from the northern Jemez. There the
Poleo Sandstone is thick and impressive, while the Shinarump
Formation, while not insignificant, is decidedly less impressive.
Here in the southern Jemez, the Shinarump has become much
thicker and the Poleo Formation has become much less significant.
In fact, there is some debate among geologists over whether the
Agua Zarca Member and the Poleo Sandstone are really the same
formation, just in different locations, interbedded with a tongue
of the Salitral Formation. However, even where the Salitral is
absent, there are subtle lithological differences between the two
Petrified Forest Formation beds are also exposed on the east side of the Rio Grande Rift, near the La Bajada Escarpment.
Petrified Forest Formation near Galisteo Dam.. 35 27.755N 106 14.049W
Here Galisteo Creek has eroded back the La Bajada Escarpment to
expose these beds.The more resistant beds capping the hills may
belong to the Correo Sandstone Member of the Petrified Forest
Formation, but this identification is uncertain.
About 201 million years ago, the supercontinent of Pangaea began to rift apart to form the Atlantic Ocean. This rifting was accompanied by a pulse of intense volcanic activity that is probably responsible for an extinction event that geologists use to divide the Triassic Period from the Jurassic Period. Though not nearly as dramatic as the "Great Dying" at the end of the Permian Period, this extinction event wiped out 20% of taxonomic families of life.
The western edge of North America continued to sit over a
subduction zone, with the associated mountain building and
volcanic activity. From about 163 to 143 million years ago, the
great batholiths of the Sierra Nevada were formed, an episode
geologists have named the Nevadan Orogeny, but northern New Mexico
was still low enough to continue accumulating sediments. These
were predominantly deposited in ergs (sand seas) around the
Sundance Sea, an arm of Arctic Ocean whose shoreline moved back
and forth across western North American throughout the Jurassic
Period. Southern New Mexico was dominated by the high terrain of
the Mogollon highlands.
There are only spotty exposures of Jurassic rocks in the southern
Jemez, but there are more extensive outcrops west of the Sierra
Nacimiento and in the northern Jemez. These become very extensive
to the northwest, across the Colorado Plateau. They reappear
southeast of the Jemez on the east margin of the Rio Grande Rift,
and extend as far east as Oklahoma.
South of Youngsville, Forest Road 100 winds south into the Jemez Mountains, past landslide deposits and outcroppings of the Petrified Forest and Rock Point Formations. Ahead is Cerro Pedernal and the mouth of "Mushroom Canyon".
This photograph shows the entire Jurassic column in the northern Jemez, which is well exposed in this area. The foreground and the bank of reddish sediments at the foot of the prominent bluff are Rock Point Formation of the Triassic Chinle Group. The bluff itself is Entrada Sandstone capped by Todilto Formation, which also appear in the slopes to the left and right. The middle skyline is Summerville Formation, with a thin rim of Morrison Formation on the ridge to the right of the prominent bluff.
Missing from the base of this column, in the 45-million-year gap
between the Rock Point Formation and the Entrada Sandstone, is the
entire Glen Canyon Group, consisting of the Wingate, Kayenta, and
Navajo Formations. Geologists believe these were laid down in a
giant dune sea that covered much of Utah, Arizona, and large parts
of Colorado and New Mexico. However, the Navajo Sandstone was
subsequently deeply eroded, and none is left in the Jemez Area.
Substantial beds still exist on the Colorado Plateau to the
Relief map of the Jemez with Entrada outcroppings highlighted in red.
Some 165 million years ago, another dune sea marched across
almost as large a region as the Navajo Sandstone. This deposited
the Entrada Sandstone, which forms many of the arches in Arches
National Monument. The Entrada Sandstone is also notable because
it finally buried the eroded remnants of the Ancestral Rocky
Mountains, some 145 million years after they first rose.
Here's a close up up of the
isolated outcropping from the mouth of "Mushroom Canyon."
The Entrada Sandstone forms the yellow beds in the lower half of
this small butte. This formation is fairly well cemented when
fresh, but it weathers quickly in this climate, so that exposed
surfaces become so soft that they easily crumble when touched. In
some parts of the Colorado Plateau, the Entrada Sandstone is
thoroughly indurated and forms prominent cliffs, while in other
areas (particular further west) it is a soft mudstone.
The road turns between two banks of Entrada Sandstone.
You can see a considerable amount of sand that has crumbled off the face of the road cut into the road bed. There is also quite a lot of grafitti scratched into the Entrada Sandstone in and around this road cut. This illustrates how weakly indurated the sandstone is in this area.
The road cut also shows obvious cross bedding. You can see this
in the large bed at the base of the road cut. Cross bedding is an
indication that the sediments were laid down in a strong current,
either of air or water. In the case of the Entrada Sandstone,
which was laid down as sand dunes in a desert environment, the
cross bedding is a consequence of strong prevailing winds. In this
case, the tilt of the cross beds suggests the wind was from the
northeast (left in this picture) consistent with other evidence
that the Jemez area lay in the trade wind belt during the
Jurassic, at a latitude about 20 to 30 degrees north of the
Here is a closer view of the butte, taken on a cloudier day, showing the Entrada beds that form its slopes.
Entrada Sandstone. 36 10.730N 106 32.615W
The lower beds of the Entrada Sandstone are pink. Above this is a
white bed, then a nearly mustard-yellow bed beneath the cap of
Todilto Formation. The pink is the original, unaltered, color of
the Entrada Sandstone, while the white and yellow zones reflect
chemical alteration from the alkaline and anoxic waters in which
the Toldilto Formation was deposited.
To the east of this bluff, the Entrada Sandstone underlies most of the hillside.
Entrada Sandstone. Looking east from 36 10.730N 106 32.615W
The soil cover and vegetation partially obscures the underlying beds, but one can make out the lower pink, middle white, and upper yellow beds of the Entrada Sandstone, the latter well exposed under a cap of grey Todilto Formation. The slopes above the Todilto forming the skyline are Summerville Formation.
The lower red beds of the Entrada Sandstone are present in the arroyo at the bottom of the canyon, and here I took a moderately fresh, well-indurated specimen from a recent rock fall.
Entrada Sandstone. 36 10.784N 106 32.481W
This is a well-sorted sandstone with considerable calcareous cement between the grains, which appear to be mostly quartz but with significant lithic fragments.
There are exposures of the Entrada Sandstone and the overlying Todilto Formation along much of the northern slopes of the Jemez Mountains, and corresponding exposures become spectacular in the Colorado Plateau country to the north. The easternmost exposures in the northern Jemez are found on the northernmost tongue of Canones Mesa, where they are dramatically offset by a strand of the Canones Fault.
Entrada and Todilto Formation offset by fault through Canones Mesa. Looking southwest from 36 14.149N 106 24.029W
Red and white beds of the Entrada Formation, capped with a thin bed of Todilto Formation, crop out on either side of a landslide down the north face of the mesa. On the east (left) the beds are thrown down at least 70 meters (200 feet) by the fault passing between the two outcrops. This fault does not displace the lava on top of the mesa, showing that this particular strand of the Canones Fault Zone has not been active in at least three million years. Further east, additional faults drop the beds to below the surface in the Rio Grande Rift.
The Entrada Sandstone north of the Jemez occasionally shows some interesting local features.
"Bluberries" in Entrada Sandstone. 36
14.849N 106 22.358W
These are calcite concretions, sometimes called “blueberries”
(though the term is more often applied to hematite concretions.)
A few feet away:
The structures in the upper right corner may be rhizoliths, a form of fossilized plant root.
Here are some more examples of possible rhizoliths from a point further south:
Possible rhizoliths or worm tubes in
Entrada Sandstone. 36
14.376N 106 22.518W
The Jurassic beds have been entirely eroded away in the western
Jemez, reappearing only on the west side of the Sierra Nacimiento.
Entrada Formation on Chinle Formation and capped with Todilto Formation, west of the Sierra Nacimineto. 35 37.455N 106 53.819W
A few remnants remain in the southwestern Jemez, on the west face of Borrego Mesa. The largest exposure is visible from Paliza Canyon.
Jurassic outcrops on Borrego Mesa. Looking from 35 41.256N 106 39.031W
The white band is the Jurassic Todilto Formation, while the red slope beneath is the Entrada Formation. Beneath are landslide deposits that include large blocks of the Jurassic formations. There is also a dramatic exposure a short distance further south, visible from the village of Ponderosa.
Entrada Sandstone on Borrego Mesa. Looking northeast from 35 39.678N 106 40.038W
The outcrop is the white patch to the left. A somewhat strenuous hike up the hills to the left gives one a closer look.
Entrada Sandstone on Borrego Mesa. 35 40..647N 106 38.539W
Additional very small outcrops of Jurassic rocks are found along the mesa for some miles south.
In the southeastern Jemez the Jurassic beds disappear into the Rio Grande Rift. They reappear south of Interstate 25 in the Hagan Basin north of the Sandia Mountains. Here Entrada Formation is exposed along La Bajada.
Entrada Formation near La Bajada. 35 27.532N 106 13.351W
There are especially spectacular exposures east of the settlement of Puertocito.
Jurassic Park. 35 16.504N 106 17.147W
The red formation at bottom is Chinle Group, probably Correo Member of the Petrified Forest Formation. Or that's what our road log tells us; I find myself wondering if this isn't the same lower red beds of the Entrada Sandstone that appear in the northern Jemez. Above is yellow Entrada Sandstone, and at top is gray Todilto Formation. All are well-indurated here. Here's a sample of the Entrada Sandstone.
Entrada Sandstone from Hagan Basin.. 35 16.504N 106 17.147W
The color and grain size are the same as in the northern Jemez, but the grains are here cemented tightly together. The grains are medium in size, mostly quartz, but with enough lithic fragments to make this a lithic arenite. You can see some of the lithic fragments as dark spots in the image.
As with the previous Chinle Group beds, the Entrada Sandstone
always rests on Chinle Group wherever it is found in the Jemez.
Thus, the paleotopography map shows no hints of high ground. This
will be true of almost every formation in the Jemez through the
remainder of the Mesozoic, a time of great tectonic stability in
northern New Mexico.
We first heard of the Washington Punitive Expedition of 1849 in
the previous chapter. After leaving Jemez Pueblo, the expedition
headed towards the general vicinity of Chaco
Canyon. Lieutenant Simpson continued his detailed
observations of the geology along the expedition's route, while
R.H. Kern produced drawings of such prominent features as Cabezon
Peak. Simpson took particular interest in the white beds of
gypsum west of San Ysidro, remnants of a shallow Jurassic sea that
briefly inundated the Jemez region.
Relief map of the Jemez with Todilto outcroppings highlighted in red.
The Todilto Formation was laid down in a geologically brief
period of time in a short-lived embayment of the Sundance Sea.
This likely formed what geologists call a barred basin.
Seawater enters a barred basin across a shallow bar like that
shown in the diagram. If the climate is hot and arid, as it was in
northern New Mexico 160 million years ago, water rapidly
evaporates from the seawater in the basin, concentrating dissolved
salts and increasing the density of the seawater. This dense brine
sinks to the bottom of the basin, where it is trapped by the
bar. As more saturated brine accumulates, substantial
amounts of evaporites begin to crystallize out of the
brine onto the floor of the basin. Meanwhile, more seawater flows
across the bar to contribute its dissolved solids to the basin.
This process can produce far greater thicknesses of evaporites
than could be produced by simply evaporating a single body of
seawater one time.
Evaporites are minerals that are more or less soluble and which
are present in significant quantities in seawater. In the early
stages of a barred basin, limestone may be deposited on the basin
floor through processes little different from those that produce
limestone in other shallow marine environments. Initially, this
limestone may include marine fossils, but as brine accumulates the
basin bottom becomes inhospitable to life. As the process
continues, additional carbonate minerals are deposited from the
brine, followed by gypsum, CaSO4.2H2O, then
halite, NaCl, then potassium and magnesium minerals.
The Todilto Formation shows the early stages of such an evaporite
sequence. There is typically a limestone bed at the base of the
formation, here named the Mesa Luciano Member, which in some
places contains fossils. For example, there is a particularly rich
bed of fossils at Warm
Springs, near San Ysidro, noted for its insects and
ostrocods (seed shrimp). The overlying gypsum is so easily
dissolved that it is missing in many locations, leaving only the
limestone. There are no halite beds; either the evaporation
sequence did not progress that far, or the halite beds have
entirely dissolved away.
We've seen several photographs showing the Todilto Formation as a
grey bed on top of the Entrada Sandstone. These beds are difficult
to get to, since they tend to be found at the top of high cliffs.
However, I was able to get fairly close to the contact in Mushroom
Canyon after some scrambling around the north wall of the canyon.
Contact of Todilto and Entrada Formation. 36 10.819N 106 32.497W
The yellowish topmost beds of the Entrada Formation are visible to lower left. Above this is the basal calcareous shale of the Luciano Mesa Member. (Calcareous shale is shale containing substantial calcite.) The thick cap on top, with a more irregular texture and visible nodules of gypsum, is the Tonque Arroyo Member. Here's a sample of the Luciano Mesa Member.
Luciano Mesa Member, Todilto Formation. 36 10.819N 106 32.497W
You can see that the rock is very thinly layered. These layers
are called varves and reflect seasonal climate change, so
that a single layer corresponds to a single year. During part of
the year, clay and organic matter settled on the bottom of the
Todilto Embayment. At other times of the year, calcite
predominated. Counts of the number of varves suggest that the
Luciano Mesa Member was deposited in a geologically brief time of
about 14,000 years.
The Tonque Arroyo Member consists of shale containing numerous nodules of gypsum and limestone. Here's an example.
The translucent part of this nodule is easily carved with a knife, but does not foam under acid; the only plausible mineral identification is gypsum, CaSO4·2H2O. The more opaque sections are both harder and foam under acid; this identifies them as calcite. In some places, the gypsum forms quite large lenses. Here is an example.
Gympsum lens weathered from Todilto Formation. 36 10.784N 106 32.481W
Note the head of my walking stick, for scale. This large gypsum
lens weathered from the Todilto Formation and is located in the
arroyo beneath. Its distinctive texture is sometimes described as
chicken wire gypsum.
The gypsum weathered from the Todilto is slightly soluble in water, and repeated wetting and drying cycles in a dry climate in loose, sandy soil with abundant gypsum produces a distinctive texture.
Gypsum-rich soil showing distinctive texture. Near 36 10.784N 106 32.481W
It is possible that the crust here also contains a cryptobiotic
film of fungi and algae. Such films are common in desert climates
but are quite delicate.
Continuing east into Mushroom Canyon, one sees how it got its name.
Mushroom Canyon at its finest. Looking east from 36 10.798N 106 32.509W
The upper yellow beds of the Entrada Sandstone form the "stems" of the "mushrooms", the Mesa Luciano Member forms the "gills", the Tonque Arroyo Member forms the "caps", and the background hills are underlain by Summerville Formation.
The road out of Mushroom Canyon climbs a hill to the contact between the Entrada Sandstone and the Todilto Formation. Though the contact is covered with loose sediments, the Todilto Formation is partially exposed.
Approximate contact between Entrada and Todilto Formations. Near 36 10.637N 106 32.885W
Mesa Luciano Member, Todilto Formation. Near 36 10.637N 106 32.885W
This is a dense, fairly hard limestone that identifies this as an
outcrop of the the Mesa Luciano Member.
At the top of the hill one gets a nice view back at "Mushroom Canyon".
If you visit this area, please be aware that the western half of Mushroom Canyon is located on private land belonging to a nature conservancy. Only the eastern half is on Forest Service land, with a barbed wire fence marking the boundary. I was careful to collect my samples from the Forest Service side.
Todilto Formation can also be visited further north, across the main highway through Abiquiu at Red Wash Canyon. No gypsum is present here, but the limestone beds remain.
Todilto Formation near Red Wash Canyon.
14.787N 106 22.471W
The deformation being pointed to likely arises from the nearby Canones Fault Zone.
Perhaps the most accessible good exposures of Todilto Formation
are found along Forest Road 77, or Mesa Alta Road, which runs to
the top of Mesa Alta. The road cuts through the Entrada Sandstone
and overlying Todilto Formation.
Here is the contact between the Entrada Sandstone and the Luciano Mesa Member.
Contact of Entrada Sandstone with Mesa Luciano Member on Forest Road 77.. 36 14.787N 106 22.471W
The contact is very sharp and the uppermost bed of the Entrada Sandstone is unusually well cemented. Some geologists have concluded from this that the Todilto Sea formed catastrophically, perhaps frrom erosion breaching a barrier between a deep basin and the open sea. Further along the road is the contact between the Luciano Mesa Member and the Tonque Arroyo Member.
Contact of Luciano Mesa Member with Tonque Arroyo Member on Forest Road 77.. 36 14.787N 106 22.471W
The Luciano Mesa Member is the thinly bedded lower section. I could find no fossils in this particular location. The massive gypsum rich beds above are Tonque Arroyo Member. Further still are some very impressive beds of massive gypsum.
Massive Tonque Arroyo Member gypsum on Forest Road 77.. 36 14.787N 106 22.471W
Note the obvious vertical fault trace in the middle of the road
cut. This is a local enough fault to not appear on the geologic
map for this area. The downthrown side is to the right and is
massive gypsum of high purity, sometimes called alabaster.
Impressive beds of the Todilto Formation are found southwest and west of the Sierra Nacimiento, where they have been exposed by the deformation that elevated the Sierra Nacimiento. The most striking of these may be Cuchilla Blanca Hill.
Cuchilla Blanca Hill. Looking east from
39.444N 106 53.547W
The hill is topped with Todilto Formation which dips sharply to the north (left). Underneath is Entrada Formation, and beneath that is Triassic upper Chinle Group red beds. The distant ridge to the right is underlain by Agua Zarca Member of the Shinarump Formation, and the ridge partially hidden behind it is underlain by more Precambrian gneiss.
Further north, the Todilto Formation is again well exposed at Cerro Blanco.
Cerro Blanco. Looking northwest from 36 13.962N 106 50.317W
Like the Entrada Formation, the Todilto Formation is absent east of the Sierra Nacimiento and north of Borrego Mesa. There are some beds along Borrego Mesa, but the first really large exposure south of the Jemez is at White Mesa. Here enough of the gypsum remains that it can be economically mined.
White Mesa. Looking northwest from near 35.48N 106.709W
The Todilto forms the white cap that gives the mesa its name.
Additional gypsum mines are located south of I-25 on the east side of the Rio Grande Rift. One of these is the Rosario gypsum mine, which exploits Toldilto beds along the La Bajada escarpment.
Rosario. Looking southest from 35 29.206N 106 15.229W
The reddish slopes at left are Chinle Group, while the yellowish
bed forming a shelf above that is the Entrada Sandstone. At right,
the Entrada Sandstone is overlain by thick beds of Todilto
Formation mined for its gypsum content. The locally thick beds may
fill a gully or other depression eroded into the surface of the
Entrada Fornation before the Todilto Formation was laid down.
The hills in the background are underlain by Jurassic Morrison
Formation under a rim of Cretaceous Dakota Formation. We'll learn
about both of these younger formation presently. The escarpment
here, the La Bajada escarpment, marks the east boundary of the Rio
Grande Rift in this region.
Relief map of the Jemez with Summerville Formation outcroppings highlighted in red.
The Summerville Formation was laid down 155 million years ago as
tidal flats and dunes. This was a time when the major rivers of
the area began slowly shifting their courses, from the southeast
to northwest flow of the Triassic and early Jurassic to the
southwest to northeast flow that would prevail throughout the rest
of the Mesozoic. This was largely a consequence of continuing
mountain building to the west and southwest (the Nevadan Orogeny),
which also emplaced the great granite masses of the Sierra Nevada.
Bone fragments and teeth of Camarasaurus, a large
herbivorous dinosaur, have been found in the Summerville Formation
in the Hagan area.
The Summerville Formation is exposed in several locations in the northern Jemez. The exposure south of Mushroom Canyon is best viewed from along the road out of the canyon.
Summerville Formation in Mushroom Canyon. Looking southeast from 36 10.662N 106 32.947W
The gray beds to the left, just peeking over the foreground ridge, are Todilto Formation. Above are the pinkish tan beds of the Summerville Formation. The very top of the ridge is a thin bed of Morrison Formation. The gray bed in the road cut to the right is Entrada Sandstone, while Cerro Pedernal looms on the skyline.
Summerville Formation is also exposed on the north rim of the canyon.
Summerville Formation in Mushroom Canyon. Looking southeast from 36 10.662N 106 32.947W
The entire skyline here is Summerville Formation. You can see that the beds dip slightly to the east (right), as do the underlying beds of Todilto Formation and Entrada Formation.
Another exposure of Summerville Formation is found just north of the Jemez, along Red Wash Canyon.
Jurassic beds east of Red Wash Canyon. 36
14.789N 106 22.261W
The canyon wall is red beds of the Arroyo del Agua Formation of the Cutler Group. This is capped with a thin bed of Shinarump and Salitral Formations and a thicker bed of Poleo Sandstone. The red to yellowish beds in the foreground are Entrada Sandstone, capped with a thin layer of limestone of the Todilto Formation. Above this to the left is a pinkish exposure of the overlying Summerville Formation. Though not well exposed, my geologic map shows that the Morrison Formation is present at the top of the hill, as well as some thin beds of Cretaceous Burro Canyon Formation.
Here's a close view of the Summerville beds.
Summerville Formation. 36
14.588N 106 22.643W
It's basically muddy sand, quite poorly cemented. It reminds me a little of the much younger Ojo Caliente Member of the Tesuque Formation, and it seems likely that exposures of the Summerville Formation were a major source of sediments for the Ojo Caliente.
There are only a few small exposures of Summerville Formation in the southern Jemez, along the west face of Borrego Mesa.
The beds immediately above the Todilto Formation south and
southwest of the Jemez tend to be assigned to the Morrison
Formation in older maps. However, more recent maps assign these
beds to the Summerville Formation, which they certainly resemble
in the area north of Chuchilla
Summerville Formation north of Chuchilla Blanca Hill. 35 39.578N 106 53.564W
The Summerville Formation extends to southern Utah, where it is often dramatic in outcrop.
Summerville Formation west of Hanksville, Utah. 38 22.279N 110 45.216W
The beds here contain considerable gypsum. Dissolution of gypsum
from the beds in the wetter climate of the Jemez may explain the
more poorly cemented beds here.
The exposure map for Summerville Formation appears to show that
it is much less extensive than the underlying Jurassic formations.
This should be taken with a grain of salt. The geologic maps
showing the next formation, Morrison Formation, lying directly on
Todilto Formation are all older maps, and many describe a lower
unit of the Morrison Formation whose description is much like that
of the Summerville Formation. It is likely that this lower unit
would be mapped as Summerville Formation if these areas were
Relief map of the Jemez with Morrison Formation outcroppings highlighted in red.
The next Jurassic formation in the Jemez is the Morrison
Formation, which is a fluvial sandstone about 150 million years
old. It was laid down as the Sundance Sea began to retreat to the
north, leaving behind a swampy lowland crossed by sluggish
streams. It is also the oldest formation in the Jemez area
composed largely of sediments eroded off the growing highlands
along the west coast of North America.
The Morrison Formation is highly variable, with up to three
distinct members mapped in some locations in the Jemez region, and
in many places it is rich in fossils, including over 70 dinosaur
species. It is a source of uranium in other locations,
particularly in the Grants area.
The Morrison Formation is exposed around Mushroom Canyon, though the exposures are not easily reached. This is as close as I could get:
Morrison Formation in upper Mushroom Canyon. Looking east from 36 10.282N 106 32.116W
Here the Morrison Formation takes the form of easily eroded
The Morrison Formation is also exposed back at the Canones fault
zone with which we began this chapter. This exposure occurs on the
east side of the fault. Here the fault has thrown up the contact
between the Morrison Formation and the El Rito Formation.
The geology in this spot is quite interesting. All the beds above
the Morrison Formation were eroded away over 50 million years ago.
Sometime between 50 and 30 million years ago, the El Rito
Formation was laid down on the erosion surface, some time prior to
the opening of the Rio Grande Rift.
The contact is clearly visible near the top of the cliff, where the beds of the two formations lie at an angle to each other. This is a good example of what geologists call an angular unconformity.
Here is a close up of the point of contact between the Morrison and the El Rito Formations, where it comes close to the road level.
This contact represents a gap in the geological record of at
least 100 million years. Here's a sample of the Morrison Formation
from this exposure.
I mentioned earlier that the Morrison Formation is famous for its fossils. Sure enough, there are biological traces in this outcropping.
The species involved is of course Homo sapiens, very
likely a college geology class practicing the skill of taking core
samples of a rock outcrop, judging from the large number of
Here is a close up of the uppermost part of the Morrison Formation, showing some very thin bedding.
The entire Jurassic and and much of the Cretaceous column of the northern Jemez is exposed on the south slopes of Mesa Alta, northwest of Coyote.
Mesa Alta. Looking north from. 36 10.954N 106 52.368W
Mesa Alta is a broad anticline, or upwards warp in the
Earth's crust, roughly aligned with the Sierra Nacimiento and
likely thrown up by the same tectonic forces. The by now familiar
Entrada and Todilto Formations form the lower cliffs of the mesa.
Above are cliffs of Summerville and Morisson Formation, capped
with Cretaceous Burro Canyon Formation and isolated hills of
Dakota Formation. The Summerville Formation forms thick beds in
the lower half of the upper cliffs, while the Morrison Formation
is more massive.
Mesa Alta. Looking north from. 36 10.954N 106 52.368W
The Morrison forms extensive and well-cemented sandstone beds west of the southern Sierra Nacimiento.
Morrison Formation west of the southern
Sierra Nacimientos 35
40.134N 106 54.756W
The Morrison Formation is famous for its varied hues, which are
evident in the beds in the lower slopes of the ridge. This is
likely the Jackpile Member of the Morrison Formation.
This is not far from the area where the giant sauropod dinosaur,
Seismosaurus, was discovered. Camarasaurus fossils
have also been found in this area.
Morrison Formation is exposed along the La Bajada escarpment south of I-25, where it forms part of the eastern boundary of the Rio Grande RIft. The road to the Galisteo Dam cuts through beds of the Jackpile Member of the Morrison Formation.
Jackpile Member of the Morrison Formation near Galisteo Dam. 35 27.306N 106 12.858W
The Jackpile Member is described as being mostly crossbedded kaolinic subarkosic sandstone (sandstone rich in clay and feldspar grains) with some beds of greenish mudstone. One such mudstone bed is obvious in this photograph.
Three members of the Morrison Formation are mapped in this area.
La Bajada escarpment near Galisteo Dam. Looking northwest from 35 27.538N 106 13.330W
The knoll left of center and below the skyline is the lowermost Salt Wash Member of the Morrison Formation, which is composed here of fairly resistant sandstone and conglomerate. Above it are the Brushy Basin Member (mostly mudstone) and Jackpile Member (mixed sandstone and mudstone), both less resistant and therefore forming a gentler slope.
The Jackpile Member is well exposed in the spillway cut for Galisteo Dam.
La Bajada escarpment near Galisteo Dam. Looking northwest from 35 27.538N 106 13.330W
The entire thickness of exposed rock is Jackpile Member, except for a very thin rim of Dakota Formation. We’re seeing this at a highly oblique angle, which exaggerates the dip of the beds to the east. However, you can see (if you click to zoom in ) that the surfaces between Jackpile beds are fairly irregular, and the beds are at a slightly different dip than the overlying Dakota Formation. The irregular surfaces between beds may be typical of fluvial deposits. The contact with the Dakota Formation is a fine example of an angular unconformity. It tells us that the Jackpile beds were already slightly tilted and partially eroded when the Dakota Formation began to be laid down.
The dip of the rocks at Poblazon is to the west, or from the Rocky mountains; and this proves that these mountains have been elevated since the deposit of the cretaceous beds. It is, therefore, probable that the cretaceous beds on both sides of the Rocky mountains were made by the same ocean.
— Lieutenant James W. Abert, 1847
The Mexican-American War of 1847 brought a virtually unopposed
invasion of New Mexico by the U.S. Army. The Army, in turn,
brought in officers of the Corps of Topographical Engineers, who
were well trained in scientific disciplines, including geology.
These officers made the first reports to the outside world of the
geology of New Mexico, previously an impoverished backwater
province of Mexico which had apparently never been visited by a
trained scientist. James W. Abert was one such officer-scientist,
who had previously (and illegally) reconnoitered the Canadian
River in northeastern New Mexico. After the U.S. Army passed
through Santa Fe, Abert and a fellow officer, Lieutenant William
G. Peck, were ordered to survey and map central New Mexico.
Among other activities, Abert visited the Cretaceous beds along
the Rio Puerco, which arises in the north Sierra Nacimiento and
runs south to join the Rio Grande north of Socorro. Abert
recognized both ammonite and Inoceramus fossils, typical
of the Cretaceous Period, and sent samples to J.W. Bailey, a
professor at West Point. Abert's observations about the dip of the
Cretaceous beds and his speculations about the existence of an
ocean covering the entire region are among the first to point to
the existence of the Western Interior Seaway, the great
epicontinental sea that invaded central North America as the Age
of the Dinosaurs began to draw to its close.
At the start of the Cretaceous, South America rifted away from
Africa, and the vigorous new mid-ocean ridge displaced enough sea
water to raise sea levels to the highest levels we know of in the
geological record. This produced coal beds rivaling those of the
Carboniferous. At the same time, vigorous subduction under the
western edge of North America began another episode of mountain
building, the Sevier Orogeny. This produced characteristic shallow
faulting in which the surface sedimentary beds detached from the
underlying basement (décollement) and rode up over younger
beds further east. The Sevier Orogeny shortened the crust in the
Nevada-Utah area by over 100 km (60 miles).
The weight of the mountains thrown up in western California and eastern Nevada caused plate flexure, where the continental lithosphere further inland was pushed down into the mantle. The flow of subducting rock downwards beneath western North America also tended to pull the crust downwards. The combined effect was to produce a deep foreland basin east of the Sierra Nevada. As the climate warmed and sea levels rose, this basin was flooded by a shallow sea, the Western Interior Seaway, in an event called the Zuni Transgression. The Jemez area was thus in a coastal or shallow marine environment during the Cretaceous, and coal beds were laid down in many locations in northern New Mexico, including the Madrid area southeast of the Jemez. The record of oceanic transgressions and regressions is particularly complete in northwestern New Mexico, where sandstone beds in the prevalent shale shows the passage of shorelines over time. The Jemez area was above sea level at the start and end of the period, but was submerged for around 20 million years in its middle.
The Western Interior Seaway is unusual in the geologic record in
that ample runoff from the mountains to the west reduced the
salinity of the water significantly. The runoff also carried
considerable organic matter, which produced many black shale
beds of the Cretaceous in the western United States. Sediment
accumulation was rapid, as much as 195 meters per million years in
some locations in southwestern Colorado.
During the Cretaceous, true flowering plants (angiosperms)
appeared and rapidly proliferated. Foraminifera and diatoms
dominated the ocean plankton and produced great beds of chalk and
chert in some parts of the world; "Cretaceous" is derived from the
German Kreide, chalk. New families of molluscs
proliferated, including the distinctive oyster-like Inoceramus.
Ammonites were also diverse and abundant, and their rapid
evolution allows beds to be correlated with high precision. The
climate was as warm as any in the geologic record, with
subtropical vegetation extending clear to the Arctic Circle.
Petrified palm stumps have been found in the upper Cretaceous near
Cuba, New Mexico, in spite of the fact that New Mexico was at
about 45 degrees north latitude, compared with 36 degrees latitude
As Forest Road 100 ascends the narrow canyon of the Rio Encino,
on the way to the La
Grulla Plateau, it passes Cretaceous rocks of the Burro
Canyon and Dakota Formations.
Cretaceous exposes in Rio Encino canyon. Looking east from 36 9.813N 106 31.990W
That's Cerro Pedernal on the skyline. The foreground cliffs are
rimmed with Dakota Formation, and the slopes beneath are exposures
of Burro Canyon Formation. Above the cliff, on the plateau, is
Mancos Formation and Tertiary El Rito Formation.
Climbing the hillside, one gets an excellent view of the opposite side of the canyon and its corresponding exposures.
The heights to the left are the northern edge of the La Grulla
Plateau. The distant mountain to their right is San Pedro Mountain,
in the Sierra Nacimiento. Mesa Montosa and Alta Mesa dominate the
right side of the panorama. The Dakota Sandstone forms the rim
visible across the entire panorama, including the distant mesas in
the final frames.
Panorama of Rio Encino canyon. 36 9.829N 106 31.878W
Relief map of the Jemez with Burro Canyon Formation outcroppings highlighted in red.
The Burro Canyon Formation was formed by braided streams along
the coastal plain of the Western Interior Seaway around 120
million years ago. Its base is placed at the first bed of
conglomeratic sandstone above the mudstone beds of the Bushy Basin
Member of the Morrison Formation.
Ascending the slopes in the previous photograph, one comes to outcroppings of this formation.
Burro Canyon Formation. 36 9.833N 106 31.876W
Burro Canyon Formation. 36 9.833N 106 31.876W
Under the loupe, this is revealed as a well-sorted sandstone composed almost entirely of angular quartz grains, with significant calciferous cement in the pore spaces -- though not enough to make it a wacke. A fairly mature quartz arenite.Nearby is another outcropping.
Burro Canyon Formation. 36 9.829N 106 31.878W
This outcrop reveals thin conglomerate beds, characteristic of the Burro Canyon Formation. For the most part, though, the exposures of Burro Canyon Formation in the northern Jemez are poor, typically mantled by soil or colluvium. My identification of these beds as Burro Canyon Formation is based on matching my GPS coordinates with the geologic map and assuming that the sandstone beds of the Burro Canyon will tend to stand out in exposure more than the mudstone beds. But it is possible I am actually looking at the lowermost beds of the Dakota Formation here, which might be assigned to the Cubero Member.
To see a decent exposure of the formation, one must look beyond
the Jemez. Here is the formation in the spillway for Heron Lake,
southwest of Chama.
Burro Canyon Formation. 36.6633573N 106.704652W
Here the alternating sandstone and gray or greenish mudstone,
reminiscent of the Jackpile Member of the Morrison Formation, are
The exposure map shows that this formation is restricted to the
northern Jemez. The formation pinches out at about the latitude of
Cuba. Since the next youngest formation, the Dakota Formation, is
found atop Morrison Formation in almost every other exposure of
Cretaceous rocks in the Jemez Area, the area north of the Jemez
may have been relatively low ground with higher terrain to the
south. This is consistent with the picture of the Burro Canyon
Formation as fluvial sandstone deposited close to the shore of the
Western Interior Seaway while the latter was still relatively
limited in extent. However, the upper surface of the Burro Canyon
Formation is an erosional surface, so it likely extended somewhat
further to the south than it is now found before being partially
All this assumes that the Jackpile Member of the Morrison
Formation and the Burro Canyon Formation are actually distinct
units. Geologists have their doubts about this, and the complete
lack of fossils in the Burro Canyon Formation in the Jemez makes
it hard to date the units precisely enough to be sure. They
certainly look a lot alike to me. And if they are the same unit,
the lack of Burro Canyon Formation mapped south of the Jemez means
nothing; the geologists are simply mapping it as something else.
Relief map of the Jemez with Dakota Formation outcroppings highlighted in red.
The Dakota Formation was deposited around 105 million years ago
in a shallow marine or mud flat environment. Its vast extent (from
Arizona to Wisconsin) reflects the full development of the Western
Interior Seaway, which completely flooded the interior of North
America in the middle Cretaceous. Its base is placed at the top of
the last greenish mudstone of the Burro Canyon Formation, or the
first bed containing carbonaceous material, whichever comes first.
Cliffs of Dakota Formation dominate the rim of Rio Encino canyon,
as we saw in the earlier photographs. Here's the formation up
Paguate Sandstone, Dakota Formatin. 36 9.859N 106 31.839W
This prominent cliff is the Paguate Sandstone, the most prominent bed of the Dakota Formation in this area. It is an extremely well-indurated sandstone, accounting for its resistance and tendency to form cliffs. Here's a sample.
Paguate Sandstone, Dakota Formatin. 36 9.859N 106 31.839W
This is similar to the Burro Canyon Formation, but the grains are smaller, better rounded, and more strongly cemented together.
The Paguate Sandstone shows significant cross bedding.
Cross bedding in Paguate Sandstone, Dakota Formation. Click to enlarge. 36 9.859N 106 31.839W
The cross bedding is evident towards the bottom of this boulder.
Like many sandstones, the Paguate Sandstone also preserves some ichnofossils,
or trace fossils.
Ichnofossils are fossil traces of living organisms that are not the
organisms themselves. Obvious examples are dinosaur footprints, some
of which have been found in other locations in the Dakota Formation.
Because trace fossils are often highly distinctive, but the
organisms that produced them may not always be known with certainty,
ichnofossils are given their own ichnogenera and ichnospecies names.
In this case, we are looking at trace fossils of the ichnogenus Thalassinoides,
which are believed to have been most commonly produced by
sediment-dwelling crustaceans. Sedimentary rocks that formed from
sediments that were extensively tunneled by living organisms are
described as bioturbated, and the Dakota Formation in
northern New Mexico is noted for its high degree of bioturbation.
Ichnofossils in Paguate Sandstone, Dakota Formation. Click to enlarge. 36 9.859N 106 31.839W
As one continues ascending into the Jemez along Forest Road 100, the road reaches the level of the Paguate Sandstone.
Unsurprisingly, this look identical to the previous sample under
The Dakota Formation also forms the lip of the La Bajada
escarpment south of I-25, as we saw earlier.
Here the Oak Canyon Member of the Dakota Formation sits directly
atop the Jackpile Member of the Morrison Formation; no Burro
Canyon Formation is mapped in this area.
The sequence of moderately resistant Morrison Formation, softer
Burro Canyon Formation, and highly resistant Dakota Formation caps
Mesa Alta, and forms long finger ridges and valleys reminiscent of
the finger mesas of the Pajarito Plateau. The Morrison Formation
underlies the valley floors while Dakota Formation (likely Paguate
Member) caps the finger ridges.
Dakota Formation atop Morrison Formation south of I-25. 35 27.357N 106 12.777W
Dakota Formation atop finger ridge on Mesa Alta. 36.2371376N 106.7418887W
Relief map of the Jemez with Mancos Formation outcroppings highlighted in red.
The Macos Shale was deposited in the Western Interior Seaway
between 95 and 80 million years ago. The area of deposition was
enormous, with equivalent shale extending well east of the Rockies
(the Pierre Shale) and to southwest Utah (the Tropic Shale.) In
places it is over 1600 meters (4800') thick. However, it rapidly
weathers in exposures to a nondescript gray to brown mud. Areas
underlain by Mancos Shale tend to quickly erode into low relief,
sparsely vegetated terrain.
Although there are exposures in the northern Jemez, they tend to be rather poor. Here is an exposure above the cliffs of Paguate Sandstone on the east side of the Rio Encino valley. The mudstone has weathered to yellowish-gray mud, mantled with basalt boulders from the La Grulla beds.
Badly weathered Mancos Shale in the northern Jemez. 36 9.859N 106 31.839W
However, there are extensive exposures in the Cerrillos
area of New Mexico, southeast of the Jemez, a historically
important mining district. In this drier climate, these are better
Mancos Shale in the Cerrillos mining district. 35 26.881N 106 7.153W
The exposures extend for a considerable distance around the Cerillos area, including well to the south and east, such as this dramatic contact in a road cut near Placitas.
Mancos Shale underlying piedmont gravels near Placitas. 35 18.013N 106 28.537W
The somewhat weathered Mancos Shale to the lower right is
overlain by piedmont gravels eroded off the Sandia uplift.
The Mancos Formation has been divided into a number of members. The most prominent member west of the Cerillos Hills is the Niobrara Member, which is divided into upper and lower sections by a distinctive sandstone bed.
Sandstone marker bed in Niobrara Member. Looking northeast from 35 28.521N 106 10.449W
This is well exposed in a road cut nearby.
Niobrara Member. 35 28.569N 106 10.502W
My wife and her brothers probably find this very familiar-looking, and not necessarily in a happy way. The Mancos Formation gets its name from its type location at Mancos, Colorado, and the stuff is all over the place, including the valley outside Pagosa Springs where my in-laws have owned a time share on a cabin for over forty years. The kids probably skinned a few knees on vacation by trying to scramble up slopes of this stuff. It is slippery and crumbly and just made to send you tumbling when you try to walk across it.
And, as I mentioned earlier, exposures tend to weather to nondescript piles of mud in geologically short intervals of time, so it isn't usually even much to look at. The most boring part of the drive from Los Alamos to central Utah, which my family made at least annually from the time we were kids clear through my college days, was the stretch between Green River and Price that passed over miles and miles of nondescript muddy Mancos Shale.But I haven't really got it in for the Mancos Shale. It's rich in fossils. It's also one of the more promising source rocks for future oil exploration, and that counts for a lot.
The best exposures in the Jemez area are west of the Sierra Nacimiento Mountains. Here's a nice exposure in a road cut.
Mancos Shale west of the Sierra Nacimiento. 35 45.838N 106 56.338W
You can see some variety in the bedding. There is a layer with some reddish limestone in the middle of the photograph, and above it are two layers richer in whitish limestone. These are interbedded with shale.
The Mancos Formation exposures west of here include some prime
fossil beds on public lands.
This fossil is likely Inoceramus, which is very common in Cretaceous rocks of the Western Interior Seaway. It resembles a modern oyster but paleontologists now believe it is a distinct lineage of mollusc.
This is an ammonite cast.
Ammonites were shelled molluscs resembling the modern nautilus, but more closely related to squids. Appearing in the Devonian, they became extinct at the end of the Cretaceous, at the same time as most families of dinosaurs. They evolved rapidly, so that well-preserved ammonite fossils are excellent index fossils useful for determining the relative ages of different sedimentary formations. For example, the start of the Cretaceous is placed at the first appearance of hte ammonite Berriasella jacobi.
Some of the bivalve shells are preserved at this fossil bed, but there are no examples where the actual shell of an ammonite was preserved; only casts. This may be because the shells are chemically different. The bivalve shells are composed of calcite, while ammonite shells are aragonite. Both are calcium carbonate minerals, but calcite is more stable than aragonite. Aragonite dissolves below a certain depth of ocean water, called the aragonite compensation depth, while the calcite compensation depth is considerably greater. This suggests that the floor of the Western Interior Seaway managed to get below the aragonite compensation depth at some point, dissolving all the aragonite ammonite shells while leaving the calcite bivalve shells intact.
The beds from which these fossils were collected are assigned to
the Juana Lopez Member of the Mancos Formation. This member is
composed of sandy limestone rather than the shale making up most
of the Mancos Formation, and may correspond to a brief interval of
drier, hotter climate in which the waters of the Western Interior
Seaway were clearer and more conducive to the kind of marine life
than generates limestone deposits.
The visit to the Santa Fe area by Jules Marcou in 1853 was not immediately followed up. Tensions were building back east between the slaveholding South and the free states of the North, and these exploded into civil war in 1861. The end of the war in 1865 was followed by Reconstruction, and the U.S. Congress did not fund further geologic expeditions to the Jemez area until 1869.
In that year, F.V. Hayden, who had studied both geology and
medicine and served as a Union medical officer during the Civil
War, led an expedition along the Front Range of the Rockies. This
covered the area from Denver to Santa Fe, and Hayden produced a
lengthy report on his observations of all aspects of geology along
his route. The chapter dealing with the Santa Fe area begins with
a description of the geology of the Los Cerrillos area, southwest
of Santa Fe. Hayden noted the presence of Cretaceous beds
containing coal, a finding of considerable interest for refueling
trains along any transcontinental railroad passing nearby. His
report describes the dip and character of the coal beds in great
detail, noting the presence of nearby igneous dikes that had
converted part of the coal to anthracite. He correctly identified
the sandstone beds beneath the coal seams as Cretaceous in age and
noted the abundance of deciduous leaf fossils, including palm
leaves, in the lowest coal seams. However, he incorrectly
identified the coal itself as Tertiary in age.
Hayden was not the discoverer of the beds, which had been mined
since 1835, but his report doubtless influenced the decision to
route the southern transcontinental railway, which became the
Atchison, Topeka, and Santa Fe Railway, close to the area.
Relief map of the Jemez with Mesaverde Group outcroppings highlighted in red.
During the mid-Cretaceous, around 84 million years ago, the
Western Interior Seaway briefly retreated from northern New
Mexico. This left a regression/transgression sequence
whose formations are assigned to the Mesaverde Group.
The retreating sea first left behind beach deposits of sand, which became the Point Lookout Formation. As the shoreline retreated, the area behind the shore became swamps in which the shales and coal deposits of the Menefee Formation were laid down. When the sea returned to the area, a second beach sand deposit became the Cliff House Formation. These formations are well exposed at La Ventana Mesa west of the Sierra Nacimiento.
La Ventana Mesa South. Looking east from 35 47.668N 106 57.388W
La Ventana Mesa is capped with resistant sandstone of the Cliff House Formation, underneath which is less resistant Menefee Formation, another resistant sandstone layer of Point Lookout Formation, and soft beds of Mancos Formation at the base of the mesa.
Near La Ventana Mesa, the Point Lookout Sandstone consists of a lower sandy shale and an upper sequence of sandstone beds.
Point Lookout Sandstone. 35 48.928N 106 58.158W
Point Lookout Sandstone. 35 50.068N,-106 58.104W
Point Lookout Sandstone. 35 50.068N,-106 58.104W
The sample shows a “salt and pepper” appearance typical of both
the Point Lookout Sandstone and the Cliff House Sandstone. The
“pepper” appears under the loupe to be lithic grains — small bits
of dark volcanic rock. This suggests that volcanoes were active
somewhere in the watershed of the rivers that drained into the
Western Interior Seaway here. These point to the existence of a
volcanic arc to the southwest, the Mogollon Highlands.
The Menefee Formation is exposed in the area around Cerillos and Madrid, where it includes thick coal beds formed in the coastal swamps. Some exposures, such as this road cut through overturned beds of the Menefee Formation, reveal a quartz arenite composed of medium, moderately rounded, moderately sorted quartz grains, with just a few lithic grains. In other words, a fairly clean sandstone.
More typical of the Menefee are exposures of shale, often carboniferous. For example, a hogback ridge near Regina in the northwest Jemez exposes carboniferous shale of the Menefee Formation.
This is part of a hogback ridge underlain by Mesaverde Group beds. Most of the rock here is from the Menefee Formation, with just a thin cover of the younger Cliff House Sandstone at left. The upper and lower parts of the Menefee Formation are coal-bearing; here, the beds are not rich enough in carbon to be worth mining, but in other locations in the San Juan Basin, great quantities of coal are mined to power the Four Corners power plant.
Notice how distinct the contact of the Menefee Formation, at right, with the Cliff House Formation, at left, is.
Middle Menefee Formation:
Notice the bits of fossilized wood in the sample.
Upper Menefee formation:
This is some not-quite-coal, shale rich in carbon but with too much clay admixture to be useful. I could not get it to ignite in a flame.
This hogback ridge extends along much of the west side of the
Sierra Nacimiento. It is prominent in the Cuba area.
Menefee Formation southeast of Cuba. 35 58.877N 106 55.055W
Movement along the Nacimiento Fault, a major fault to the east,
has deformed the beds so much that they are slightly overturned
here, with the Cliff House Sandstone to the left underlying the
older Menefee beds to the right. The formations are also
significantly thinner here, close to the Sierra Nacimiento, than
at La Ventana Mesa. This suggests that the Sierra Nacimiento was
already beginning to be uplited at the time of the Mesaverde
The retreat of the sea in the middle Cretaceous was only
temporary. The return of the sea deposited another layer of beach
sand, the Cliff House Sandstone. We saw photographs of this in the
previous section, capping the Menefee Formation. Here's a sample
from the road cut shown there:
This is a moderately well sorted sandstone, with angular grains and many lithic fragments. Not a particularly mature sandstone.
Here's the Cliff House Formation north of Ventana Mesa, where the road approaches the formation.
Cliff House Formation north of La Ventana Mesa. 35 51.572N 106 58.303W
The mesa is capped with Cliff House Formation, over softer beds of Menefee Formation. Blocks of Cliff House Formation have broken off and litter the lower slopes, where they can be sampled.
Cliff House Formation north of La Ventana Mesa. 35 51.572N 106 58.303W
This sandstone is dirtier than the Point Lookout Sandstone. It is
richer in the “pepper” lithic grains, and it has considerable
content of feldspar grains, now weathered into clay nodules. I saw
no feldspar grains in the Point Lookout Sandstone. These suggest
that granitic bedrock was exposed somewhere in the watershed by
this point in time — about 75 million years ago.
Relief map of the Jemez with Lewis Formation outcroppings highlighted in red.
With the return of the sea, marine shale began to be laid down
again, closely resembling that of the Mancos Formation except for
its marker fossils and stratigraphic position. This is the Lewis
Shale. It is exposed southeast of Cuba
and south and southeast of Portales Mesa
Lewis Shale southeast of Portales Mesa. Near 35 52.294N 107 00.508W
I am sometimes pretty down on marine shales, which tend to form low, drab hills that turn into mud at the least excuse, but darned if the beds here aren’t almost pretty. On the other hand, it is not nearly as rich in fossils as the Mancos Shale.
Here is an exposure in a road cut.
Lewis Shale. 35 53.496N 106 58.619W
Notice the distinctive "popcorn" texture of the weathered surface. This is characteristic of sediments containing large quantities of bentonite, which we learned in the last chapter is clay rich in the mineral, montmorillonite. This form of clay expands significantly when it is moistened and shrinks when dry, which produces the popcorn texture. Popcorn texture is common in the Mancos Shale, but seems more so in the Lewis Shale.
Here is a sample from southeast of Portales Mesa.
Lewis Shale southeast of Portales Mesa. Near 35 52.294N 107 00.508W
This sample is calcareous shale (or shaly limestone) interbedded
with the more predominant muddy shale of the Lewis Formation. A
notable feature of these beds is the almost complete absence of
In addition to surveying part of the Colorado Plateau in
1873-1875, G.K.Gilbert gave some of the first accurate
descriptions of the mountain ranges bordering the Colorado Plateau
in New Mexico. Gilbert realized that the Sandia Mountains were a
fault block: "a great, but simple, monoclinal mass, bounded on the
west by a profound fault, along the line of which is the river
valley." He estimated the displacement along the fault on the
western face as at least 11,000' (3,300 m), not much less than the
modern estimate. Gilbert concluded that the Rocky Mountains had
been uplifted only after the end of the Cretaceous. Gilbert was
only a little off: The first stirrings of the Laramide Orogeny
were in the late Cretaceous, and the effects were not felt in the
Jemez region until near the start of the Tertiary.
The Lewis Shale was laid down around 72 million years ago. By this time, the Jemez area had been tectonically quiet since the Ancestral Rocky Mountains were thrown up, 300 million years earlier, and so had experienced 230 million years of slow accumulation of sediments on the basement rock. However, the slow subsidence of the area was beginning to reverse, due to tectonic changes leading to the Laramide Orogeny.
Some 124 million years ago, just before the Burro Canyon Formation began to be laid down in New Mexico, a mantle plume rose into a triple junction located somewhere southwest of North America. This was the meeting point of the Pacific Plate, the Farallon Plate, and a third plate, the Izanagi Plate, The plume was composed of unusually hot mantle rock, likely derived from a slab of oceanic crust that subducted much earlier in the Earth's history. Because oceanic crust is enriched in potassium compared with mantle rock, and potassium is very slightly radioactive, subducted crust tends to become hotter than the surrounding mantle rock. The hot rock of the plume enhanced the magma production already taking place at the triple junction, creating a vast underwater plateau.
Because the plateau was formed over the triple junction, it soon
rifted into three sections. One section still exists today as the
Shatsky Rise, a group of three underwater massifs located in the
deep ocean basin midway between Hawaii and Japan. Another section
likely was carried into Mexico. The third is thought to have been
subducted under western North America, starting around 80 million
Oceanic crust of the Farallon Plate had been subducting under the western margin of North America since the Antler Orogeny of the Mississippian. The subduction zone was much like most subduction zones seen today, with the subduction crust going into the mantle at an angle around 45 degrees. However, the thickened oceanic crust created by the Shatsky plume made the plate more buoyant, and it began to subduct at an unusually shallow angle, less than 25 degrees.
This put powerful compression forces on the overlying crust. The
crust began to buckle, becoming deeply faulted and throwing up
high mountains separated by deep basins. Most of the mountain
ranges we see in New Mexico today formed along fault lines
established during the Laramide Orogeny. The shallow subduction
also produced volcanism far inland from the continental margin.
This began sweeping east around 70 million years ago, producing
volcanic fields in what is now southwestern New Mexico (the
Mogollon-Datil volcanic field) and other locations in western
North America. This burst of volcanism is known as the
mid-Tertiary ignimbrite flareup.
The beginning of the Laramide Orogeny marked the end of the
Western Interior Seaway, which began its final retreat to the
Relief map of the Jemez with Pictured Cliffs Formation outcroppings highlighted in red.
The final regression of the Western Interior Seaway, around 77
million years ago, is marked by the Pictured Cliffs Formation,
another sandstone bed. This formation is mapped in the Cuba area,
but it is very poorly exposed compared with the thicknesses to the
north, in the Mesa Verde area. This formation is not particularly
well cemented in this area and rarely forms the hogbacks or mesa
caps formed by other sandstone formations. There are poor
exposures at the foot of Mesa Portales, just west of the Jemez
Mesa Portales, Looking northwest from 35 53.658N 106 58.497W
The mesa exposes the upper column of the Cretaceous in this area. In the foreground is Lewis Shale, while the Pictured Cliffs Formation is found at the very foot of the mesa. Above this formation are the Fruitland and Kirtland Formation, while the mesa cap is the Ojo Alamo Formation, thought to straddle the Cretaceous-Tertiary boundary.
Part of the difficult is that, in the Cuba area, the Pictured Cliffs Formation seems to consist largely of sandy shale, difficult to distinguish either from the underlying Lewis Formation or the overlying Fruitland Formation. For example, the geologic map places this road cut squarely in the Pictured Cliffs Formation
Pictured Cliffs Formation or Lewis Shale? 36 01.641N 106 55.964W
but this looks like a fine exposure of shale of the Lewis
This deep telephoto shot looks at a sequence of increasingly
older beds tilted by the Nacimiento Fault.
Pictured Cliffs Formation in middle distance. 36 00.597N 106 56.318W
The white beds at center are the Fruitland and Kirtland
Formations. The brownish ridge behind is mapped as Pictured Cliffs
Formation. Beyond that is a melange of distorted beds of Lewis
Shale and Mesaverde Group disturbed by the Nacimiento Fault.
Beyond the fault are red beds of the Abo Formation lapping onto
the San Pedro Quartz Monzonite that underlies much of the northern
Relief map of the Jemez with Kirtland and Fruitalnd Formation outcroppings highlighted in red.
With the retreat of the sea, New Mexico again was covered with
coal swamps, and coal beds in the Fruitland Formation are mined in
the Four Corners area. There are spectacular exposures of
the Fruitland Formation in the Bisti/De-Na-Zin
Wilderness Area in the San Juan Basin west of the Jemez
area. These include bright red beds of cinder, formed when coal
was ignited by lightning or wildfire and heated the surrounding
rock to high temperature.
The formations are exposed along Route 126 southeast of Cuba.
These are the youngest Cretaceous formations in the San Juan Basin. They’re lumped together on the geologic map of this area which, as you might guess, means they’re hard to tell apart in the field. I don’t know which is which here.
The Fruitland/Kirtland Formations are often capped with resistant Ojo Alamo beds in the Cuba area.
Fruitland and Kirtland Formations capped with Ojo Alamo Formation. 36 01.630N 106 56.223W
The end of the Cretaceous was marked by the most famous and
second most destructive mass extinction in the fossil record.
Unfortunately, no record of this is preserved in the Jemez area,
because the uppermost Cretaceous and lowermost Tertiary beds were
destroyed in the birth of the Rocky Mountains during the Laramide
Next page: The end of (most of) the
dinosaurs and the rise of the mammals
Copyright ©2014-2017 Kent G. Budge. All rights reserved.