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Chiricahua Mountains
Vivian Lewis
Physical Geology
Fall 2005

                         Hiking in the Chiricahua National Monument, Arizona

 

     Twenty-seven million years ago during the Tertiary age, from a caldera of a resurgent volcano in the southeastern corner of what is now known as Arizona; eruptions occurred.  Over a long period of time, ash from the Turkey Creek Caldera (Marjaniemi xvi) was spewed out in the form of air flows and pyroclastic flows.  The ash hardened into an igneous rock known as rhyolite.  At Chiricahua National Monument, the Rhyolite Canyon layer is about 1,000 feet thick and is the youngest (Marjaniemi xvi).  As the layers increased in height; they slowly cooled, and compaction, assisted by heat, rain, and freezing temperatures, attacked the hardened flows, causing the rhyolite to separate and pillar-like columns known as tuff formed (Bezy 9).


 

            In the last few millennia, man has discovered this wonderland of rocks and used this area for various reasons while admiring the numerous and sometimes bizarre formations.  In 1924, what is now known as the Chiricahua National Monument was set aside for all mankind to enjoy.  But what are the unusual shapes called and how were they formed?  On this virtual journey, we shall find out. 
 

            As with any hike in Arizona we will be at a high altitude.  Take plenty of water and electrolyte replacements in the form of liquids and snacks.  Always pace yourself; leave plenty of time to hike and enjoy the scenery.  We will start at the top of the Monument and return to our vehicle at the Visitor Center Parking lot.
 

            Our park ranger is dropping us off at the parking lot for Sugar Loaf Mountain.  The top of this mountain is formed of the youngest rock, a lava flow that came from the Turkey Creek caldera millions of years ago (Bezy 20).  Except for the mountain peak, the dacite has eroded away.  Hiking upwards, we come to our first wonder, an arch  carved by the Civilian Conservation Corps (CCC) when they built the trails in the Chiricahua National Monument in the 1930’s during the Great Depression. The arch, the buildings, the roads, the trails; all the rock fortifications that we are seeing before us, were done during that time period.  Just past the arch, to the left we see an ancient steam vent called a fossil fumarole.  Look to your right and you will see rock spires geologists call welded tuff.


 

            Dr. Darwin Marjaniemi, who in 1969, researched and located the source for all the rhyolite in the Chiricahuas, defined in his thesis, welded tuff as, “a rock or rock body in which vitric particles have some degree of cohesion by reason of having been hot and viscous at the time of their emplacement.”(Marjaniemi 3)  The best examples of welded tuff are located in the Monument.
 

 Further up, we have come to an overhanging area that is to our left.  The closest layer to us is very chalky, grey almost white.  It flakes easily and when placed in water, breaks down.  When it was dry, it crumbled to the touch.  This is known as a surge bed.  It was formed by hot fiery rock and gases that flowed down the slopes of the caldera (Bezy 18).  In the winter of 2001, I tried to hike to the top but found it was closed due to a landslide caused by a lot of rain and snow.  The slope was overloaded with moisture and weight, undercut for the trail, so the slope collapsed. The Park Service has since repaired it.



     When you walk past it, look back and you will see a fossil fumarole.    Surrounding us are the shrubs of the Mexican Locust Bean.  They have very sharp thorns and lovely gold- colored leaves in autumn.




 

At last we have hiked up to the top and we see the fire lookout.  The view all around is spectacular.  To the West we can see the Sulphur Springs Valley and the Dragoons with Cochise Stronghold.  To the Northwest we observe a large white area that is the Wilcox Playa, the remains of an ancient lake called Lake Cochise( Bezy 22).  The shallow lake had water during the last ice age that supported pines, as well as fauna such as the mammoth, horse, and camel, until about 10,000 years ago when the climate became more arid.  To the south you will notice the tallest peaks in the Chiricahuas.  That is the Turkey Creek caldera.  A thousand times more ash and rock as well as lava, was ejected from this volcano than was released from Mt. St. Helens in 1980 (Bezy 21).   
       

After hiking back down the trail, we walk along the drive to get to the Echo Canyon Parking Lot.  To the northeast, we notice an unusually shaped peak.  This is the Head of Cochise.  It is the remains of a rhyodacite flow and shaped by erosion.



       We are traveling on the Echo Canyon trail with views of Sugar Loaf Mountain on our right.  Tall, silent sentinels of stone surround us on almost all sides.  Many of them are rounded off at the corners, others have horizontal lines or ribs incised into the rock.  Soon, to our right is Echo Grotto.  The welded tuff seems to be leaning toward a center point, leaving an open space. 



     Our trail becomes a series of switchbacks and descends down among the tuff.  We come out into an open area surrounded by skyscrapers made of tuff, or if we use our imagination, we could see giant Easter Island statues.



         As we follow the trail, it narrows until we are walking between two towering walls of stone, the beginning of Wall Street.  If the hiker will look up, you will see huge vesicular-looking cavities geologists call case hardening.  The interior of the holes have a protective coating of silica that has extruded from the interior of the tuff.  According to John V. Bezy , who works for the National Park Service, ”The silica then is reprecipitated on the surface.” (Bezy 29)  In Figure 5, above the case hardening, we notice some small holes known as tafoni.  Found along the cracks or joints, this is another weathering process similar to case hardening.  They are more likely to be seen in the desert, but are indicators of a past cooler, wetter climate.



     After exiting Echo Park, an area with more trees than we have usually seen, we see an open space that is clearly a canyon.  We can see trails running parallel to the canyon and it is time to make a decision.  Which trail to take?  We decide to hike to the Heart of Rocks.  Now the trail is almost flat.  After a mile, we pass a mass of grey balls about the size of an ordinary marble.  This segment of the Rhyolite Canyon Trail is known as the Hailstone Trail.  They are not fossilized hailstones; but formed as the ash sheet cooled, crystals of feldspar and quartz fanned out in almost equal directions (Bezy 32).  As we walk past the columns of stone, we notice that many are wide at the base, narrow at the center and begin to spread out again at the top.  Others are wide at the base and narrow at the top.



      Others are narrow at the base and then widen a lot at the top.  Many seem to do a balancing act.



      To the left is the huge balancing rock.  Looking down we notice a trail of painted brown footprints, so we follow in the footsteps of past hikers as we are guided into the Heart of Rocks.  The welded tuff, composed of various ash flow layers of rhyolite, seem to be carved into familiar fantastic shapes here on this wind-swept plateau.  The generation of the Great Depression gave the tuff such names as Punch and Judy, Duck on a Rock, Thor’s Hammer, etc.  But each generation may see something different.



    In addition to the painted footprints, there are the stone staircases.  All too soon, you have come out of the Heart of Rocks, and we begin our descent down the Sarah Deming trail to the Visitor Center.  Although the hiker can not see much in the way of welded tuff during this part of the hike, toward the end of the Sarah Deming trail, there is an unusually tall spire of welded tuff that seems to soar out of sight.  At the trailhead, we look back from whence we came, and then across the canyon to see the tributaries of Rhyolite Canyon.  Across the Canyon, the hiker can see three distinct layers of what is known as Rhyolite Canyon Welded Tuff Formations (Marjaniemi 18-20).  Walking through the conifers, we can see our vehicle in the distance.


 

After the violent volcanic eruptions quieted down; Basin and Range block faulting caused the hardened ash flows to uplift, tilt, shift, crack; forming joints.  Rainwater, wind, freezing temperatures, trees and other plants also joined in the weathering and erosion of the Chiricahuas until almost twenty-seven million years later, the land continues to shape itself into the wonderland of rocks we all have come to love.

           

                                              

 

              Works  Cited

 

Marjaniemi, Darwin, PhD. “Geologic History of an Ash-Flow Sequence and Its Source Area

 In the Basin and Range Province of Southeastern Arizona”.  1969,xvi-171.

 

Bezy, John V. National Park Service. “Rocks in the Chiricahua National Monument and the

Ft. Bowie National Historic Site”.2001. 7-33