Simplified geologic map of the Raton-Clayton volcanic field (after Luedke and Smith, 1974).
View south overlooking the Raton-Clayton volcanic field from the rim of Capulin Volcano's summit crater. Photo L. Crumpler
The Raton-Clayton volcanic field (RCVF) is an excellent example of a large volcanic field. Volcanic fields differ from the more popular conception of volcanoes, like Hawaii or Mount St. Helens. Instead of one big volcano, volcanic fields consist of clusters of many small volcanoes (up to 2 miles across). Thousands of years may seperate the eruption of each small volcano, but they all occur within the space of a hundred miles or so, and are restricted to several hundred thousand to a million years in time. At any one time during the field's active lifetime, this means that it probably looked much as it does today. Each volcano consists mainly of cinders, spatters, and dark lava flows, although other types are present in many fields, the RCVF is mostly small scoria cones and associated lava flows.
The field covers nearly 7500 square miles of northeastern New Mexico and adjoining Colorado and Oklahoma. The distinctive characteristic of the Raton-Clayton field is its great size, young age, continental interior setting, and possible association with one of the few volcanic hot spots in the world. If you start traveling east, you would not encounter volcanic rocks this young again until the mid-Atlantic ridge. The lava compositions are also somewhat unusual. And it is the site of Capulin volcano, the easternmost young and easily accessible volcano in North America.
The Raton-Clayton volcanic field is best known to historians as the site of some of the best preserved segments of the Santa Fe trail. Famous landmarks on the trail such as Round Mound, Wagon Mound, and Rabbit Ears Mountains are all volcanic centers. The field is of note because it lies at the northeastern end of the “Jemez lineament”, a prominent alignment of volcanic fields extending from the Pinacate field of Mexico, through the Springerville field on the southern margin of the Colorado Plateau in eastern Arizona; the Zuni-Bandera field and the Mount Taylor fields near Grants, western New Mexico; the Jemez field and Cerros del Rio fields near Santa Fe; and terminating in the northeastern corner of New Mexico in the Raton-Clayton field. Because the alignment of fields in the Jemez lineament is parallel to the Snake River-Yellowstone volcanic hot spot track, the Jemez Lineament has been considered by some volcanologists to be a type of volcanic “hot spot”. Hot spots are rare, unlike the very common and explosive type of volcanoes like Mount St. Helens. Only 49 volcanic “hot spots” are recognized by volcanologists in the world. A few other famous volcanic hot spots include the Azores, Reunion Island, Iceland, Hawaii, and parts of East Africa.
The oldest rocks range from about 9 million years old, and the youngest erupted as little as 45,000 years ago. The earliest lavas of the Raton-Clayton field flowed onto the surface of sediment shed eastward from the Sangre de Cristo Mountains. Continuing uplift during eruption resulted in the erosion of this surface where it was not capped by volcanic rocks. During subsequent eruptions, lava flowed down valleys cut between the lava caps. The result is a series of “inverted topographic valleys” such that the oldest volcanic rocks are now found at the highest elevations above present erosional levels, with younger lavas at progressively lower levels. The most recent volcanic activity occurred at several volcanoes in the center of the field in the vicinity of Capulin Mountain, where lava flows have moved down current drainages.
The Raton-Clayton volcanic field is the easternmost Cenozoic volcanic field in the United States. To the east, Cenozoic volcanic rocks are not encountered at this latitude again until the mid-Atlantic ridge. As an interesting note and insight into the absence of appreciation of local geologic features common in most areas of the world: The town of Clayton publicizes the nearby occurrence of dinosaur tracks at Clayton Lake State Park, yet ironically makes no mention of its location near the eastern end of one of the easternmost, young, and largest volcanic fields in the North American continent.
View of Capulin Volcano National Monument from the air. Photo L. Crumpler
The youngest volcanic activity occurred in the center of the field in the vicinity of Capulin Volcano, the eastern-most young volcano in the United States. Recent work by geologists from the College of Santa Fe, Northern Arizona University, and the Park Service (Sayre et al, 1995; Stroud, 1996), yielded age dates showing that Capulin volcano erupted approximately 56,000 to 62,000 years ago, somewhat older than the reported age of the famed Folsom paleosite (~11,000 years ago). Capulin Mountain is a classic cinder cone with associated small volumes of lava flows. It is similar in size and morphology, and probably eruptive characteristics, to Paricutin volcano, Mexico which erupted in 1943.
A detailed study of Capulin (Ort, 1997), indicates that a complicated series of lava flows and cinder/spatter eruptions occurred, during or after the eruption of the cinder cone, in order to build Capulin volcano. Lava flows traveled down what are essentially modern drainages. Three major series of lava flow units occurred, the earliest flowed to the east-southeast of the cone, the second to the west and south, and the third to the west and north. The second and third series of flows erupted from an area at the base of the cone called the boca (mouth) and during these eruptions several intermittent lava lakes formed at the lower flanks of the volcano and portions of the cone were "rafted" away on the surface of the flows.
Capulin ( New Mexico) and Paricutin ( Michoacán, Mexico) volcanoes as viewed in comparable profiles and distances.
The similarity between Capulin and Paricutin volcanoes is striking. In addition to the size and general morphology of the cones, both cones developed large “bocas” or flows that emerge from one flank, that ramp up onto the cone flanks in approximately the same way and spread lava flows in much the same way. A large lava channel on the Paricutin boca is similar to the channel that today is the picnic area at Capulin. However, Capulin Volcano National Monument was created decades before Paricutin erupted. In fact, Paricutin erupted in a Mexican farmer’s cornfield in 1943, 60,000 years after Capulin.
Shadow cast toward the northeast horizon at sunset in January as seen from the summit of Capulin Volcano. Photo, L. Crumpler
Sierra Grande as seen from a southeast-directed view on the crater rim of Capulin volcano. Photo L. Crumpler
Additional Information about the Raton-Clayton field
The Raton-Clayton volcanic field lies at the northeastern end of the "Jemez lineament", a prominent alignment of volcanic fields extending from the Pinacate field of Mexico, through the Springerville field on the southern margin of the Colorado Plateau in eastern Arizona, the Zuni-Bandera field, the Mount Taylor field, the Jemez field, and Cerros del Rio Field, and terminating in the northeastern corner of New Mexico in the Raton-Clayton field (Figure 1A & B). Some studies also include the Taos volcanic field as part of the general trend as well. In fact, the Taos field bears many similarities with the Raton-Clayton field in terms of age, morphology of silicic vents, and compositions. Because the alignment of fields in the Jemez lineament is parallel to the Snake River-Yellowstone hotspot track, the Jemez lineament also has been considered by some to be a type of hot spot. As such the Raton-Clayton "hot spot" is one of only 49 hot spots identified on Earth. It should be clarified that the status as a true hot spot is not clear-cut largely because there is no strong age progression, for example, from southwest to northeast, as is typical of true hot spot tracks.
There are many volcanic fields of late Cenozoic age throughout the Southwest, each of which is distinctive in terms of the details of petrology, timing of eruptions, size, and morphology of vents, and character of pyroclastic deposits. But overall, they are all characterized by many small centers of eruption (one to a few kilometers across) of fundamentally basaltic, but ranging to more silicic, compositions. Instead of one big volcano, volcanic fields are typically on the order of one hundred kilometers across, and contain from several tens of vents to several hundred volcanic vents erupted over a period of several million years. Volcanic fields also differ from single large volcanoes, like Hawaii or the large volcanoes of the Cascades. They are also characterized by low rates of magma eruption, typically an order of magnitude less than large volcanoes.
The Raton-Clayton field is elongated northwest-southeast, the axis extending from near Trinidad, Colorado, 140 km southeastward to Clayton, New Mexico (Dungan, et al, 1989). Including the outlying parts, the field covers nearly 20,000 km2 (Figure 3) (Stormer, 1987; Muehlberger, et al, 1967). The oldest rocks range from about 9 Ma and the youngest erupted less than 60,000 years ago (Sayre et al, 1995; Stroud, 1996). The distinctive characteristic of the Raton-Clayton field is the presence of highly alkalic mafic lavas with SiO2 contents as low as 36%. However, the field also contains centers, such as Sierra Grande, that erupted andesite, dacite or rhyodacite (up to nearly 70% SiO2).
Phases of Volcanic Activity (Stratigraphy) in the Raton-Clayton Volcanic Field
Traditionally the RCVF has been divided into three main phases of volcanic activity (Baldwin and Muehlberger, 1959; Muehlberger, et al, 1967). As a result of recent age radiometric determinations (Stroud, 1996), the ages of these phases are now known to be older than reported in earlier published accounts. Nonetheless, the basic stratigraphy remains adequately defined by three periods. (Note: The following is from Mathis, 1997.)
Raton Phase 9.0 - 3.5 Ma
Clayton Phase 3.0 -2.25 Ma
Capulin Phase 1.7 - 0.04 Ma
These are defined in part by a sequence of inverted topography in which the older units are situated on earlier and now higher erosion surfaces, and subsequent eruptions were emplaced on younger and lower surfaces.The earliest lavas of the Raton-Clayton field flowed onto the surface of an alluvial apron of sediment shed eastward from the Sangre de Cristo Mountains (which are to the west of the field) (Baldwin and Muehlberger, 1959; Dungan, et al, 1989). Continuing uplift during eruption resulted in the erosion of this surface where it was not capped by volcanic rocks. During subsequent eruptions, lava flowed down valleys cut into this surface. The result is a series of "inverted topographic valleys" such that the oldest volcanic rocks are generally found at the highest elevations above present erosional levels, with younger lavas at progressively lower levels and in modern drainages. Thus the field is characterized by a kind of inverted stratigraphy.
The rate of downcutting has been significantly greater in the western part of the field along the head of valleys draining into the Canadian River. The high, lava-capped mesas in the distance to the north are over 700 m above the valley floor. To the east, the elevation of the older basalt-capped mesas decreases, and at Clayton they are only a few meters above the present valley floors.
View Raton-Clayton Volcanic Field in a larger map
General Reference Information
Petrology/ General Geology:
Anderson, A.D. and Haynes, C.V., Jr., 1978, How old is Capulin Mountain? Correlation between Capulin Mountain volcanic flows and the Folsom type site, northeastern New Mexico in Shelton, N. ed., Proceedings of the First Conference on Scientific Research in the National Parks, p. 893-899.
Andrew, J., 1997, Volcanic history of the northern Chain of Craters: in Mabery, K., (ed), Natural History of El Malpais National Monument: New Mexico Bureau of Mines and Mineral Resources, Bulletin 156, p. 31-39.
Aoki, K-I., 1967, Alkaline and calc-alkaline basalts from Capulin Mountain, northeastern New Mexico, U.S.A.: Japanese Association of Mineralogists, Petrologists, and Economic Geologists Journal, v. 58, p. 141-151.
Aubele, J. C., and Crumpler, L. S., 2001, Raton-Clayton and Ocaté volcanic fields. New Mexico Geological Society 52nd Field Conference Guidebook, p. 69-76.
Baldwin, B. and Muehlberger, W.R., 1959, Geologic Studies of Union County, New Mexico: in New Mexico Bureau of Mines and Mineral Resources Bulletin 63, 171 pp.
Calvin, E.M., 1987, A review of the volcanic history and stratigraphy of northeastern New Mexico, the Ocaté and Raton-Clayton volcanic fields: New Mexico Geological Society, 38th Field Conference, Guidebook, p. 83-85.
Collins, R. F., 1949, Volcanic rocks of northeastern New Mexico. Geological Society of America Bulletin, v. 60, p. 1017-1040.
Gust, D., 1990, Raton-Clayton, NM; in Wood, C.A. and Kienle, J. Jr., (eds), Volcanoes of North America: Cambridge University Press p. 292-293.
Jones, L.M., Walker, R.L. and Stormer, J.C., Jr., 1974, Isotope composition of strontium and origin of volcanic rocks of the Raton-Clayton district, northeastern New Mexico: Geological Society of America Bulletin, v. 85, p. 33-36.
Kudo, A.M., 1976, A review of the volcanic history and stratigraphy of northeastern New Mexico: New Mexico Geological Society, 27th Field Conference, Guidebook, p. 109-110.
Muehlberger, W.R., 1955, Relative age of Folsom Man and the Capulin mountain eruption: Geological Society of America Bulletin, v. 66, p. 1600-1601.
Muehlberger, W.R., Baldwin, B., and Foster, R.W., 1967. High plains northeastern NM; Scenic Trips to the Geologic Past, no. 7: New Mexico Bureau of Mines and Mineral Resources, 107p.
Phelps, D.W., Gust, D.A., and Wooden, J.L., 1983, Petrogenesis of the mafic feldspathoidal lavas of the Raton-Clayton volcanic field, NM: Contributions to Mineralogy and Petrology, v. 84, p. 182-190.
Sayre, W.O, Ort, M.H. and Graham, D., 1995, Capulin Volcano: Park Science, v.15, n.2, p.10-11.
Scott, G.R., Wilcox, R.E., and Mehnert, H.H., 1990, Geology of volcanic and subvolcanic rocks of the Raton-Springer area, Colfax and Union Counties, NM: U. S. Geological Survey, Professional Paper 1507, 58p.
Staaz, M. H., 1985, Geology and description of thorium and rare-earth deposits in the Laughlin Peak area, Colfax County, New Mexico: U. S. Geological Survey, Professional Paper 1049-E.
Staaz, Mortimer H., 1986, Geologic map of the Pine Buttes quadrangle, Colfax County, New Mexico. U. S. Geological Survey Map GQ 1591, 1:24000.
Stobbe, H. R., 1949, Petrology of volcanic rocks of northeastern New Mexico. Geological Society of America Bulletin, v. 60, p. 1041-1093.
Stormer, J. C., Jr., 1972, Mineralogy and petrology of the Raton-Clayton volcanic field, northeastern New Mexico. Geological Society of America Bulletin, v. 83, p.3299-3322.
Stormer, J. C., 1972, Ages and nature of volcanic activity in the southern High Plains, New Mexico and Colorado: Geological Society of America, v. 83, p. 2443-2448.
Stormer, J.C., 1987, Capulin Mountain Volcano and RCVF, northeastern New Mexico: Geological Society of America Centennial Field Guide, Vol. 2, Rocky Mountain Section, p. 421-424.
Stroud, J.R., 1996, The volcanic history and landscape evolution of the RCVF [M.S.. thesis]: New Mexico Institute of Mining and Technology, Socorro, NM, 49p.
Trauger, F.D., 1973, K-Ar dates on a basalt flow and vent plug in northeast Harding County, northeastern NM: Isochron/West, no.7, p. 7-9.