Skip to main content
SpringerLink
Log in

The Santa Fe Intrusion and Other Magmatic Bodies Under the Chichón Volcano Area (Mexico): Inferences from Aeromagnetic and New Petrologic-Geochronologic Data

  • Published:
Surveys in Geophysics Aims and scope Submit manuscript

Abstract

We review the current knowledge of the Pleistocene Modern Chiapanecan Volcanic Arc (MCVA). This arc is related to the subduction of the Cocos plate beneath the North American plate in the State of Chiapas, southeastern Mexico. The MCVA consists of large intrusive bodies, domes, eroded volcanic landforms, and the active El Chichón, which produced the disastrous 1982 eruption, the deadliest in Mexico’s recorded history. The available geological knowledge, and new geological and aeromagnetic data on the arc, reveals a system composed of a sizeable intrusive body called the Santa Fe diorite, and small-size volcanoes such as El Chichón and Catedral, and extinct volcanoes associated with volcaniclastic deposits. A 3D-inversion of the aeromagnetic anomalies indicates that the Santa Fe diorite is a large intrusive body (27 km long, 4 km wide with a minimum volume of 1662 km3) while small volcanoes such as El Chichón have small-size magma chambers (~ 7 km3). Interestingly, our models of the causative bodies for the aeromagnetic anomalies suggest that the El Chichón volcano, as well as of other volcanic areas in the region, are not linked directly to the Santa Fe intrusive. However, new 40Ar/39Ar dates for samples from the Santa Fe intrusive (2.2 Ma), the Catedral volcano (1.6 Ma), and a mafic enclave (1.09 Ma) hosted in 1982 Chichón deposits, along with the aeromagnetic anomalies and geochemical data confirm that these extrusive and intrusive structures belong to the MCVA. The chemistry of these structures suggests that magmas generated in the upper mantle by the subduction system evolved through different processes, such as crustal contamination for the Santa Fe diorite and Catedral volcano, and crystal fractionation for El Chichón volcano.

This is a preview of subscription content, log in via an institution to check access.

Access this article

Log in via an institution

Price excludes VAT (USA)
Tax calculation will be finalised during checkout.

Instant access to the full article PDF.

Institutional subscriptions

Fig. 1
Fig. 2
Fig. 3
Fig. 4
Fig. 5
Fig. 6
Fig. 7
Fig. 8
Fig. 9
Fig. 10
Fig. 11
Fig. 12
Fig. 13
Fig. 14
Fig. 15

Similar content being viewed by others

References

  • Andrews BJ, Gardner JE, Housh T (2008) Repeated recharge, assimilation, and hybridization in magmas erupted from El Chichón as recorded by plagioclase and amphibole phenocrysts. J Volcanol Geotherm Res 175:415–426

    Article  Google Scholar 

  • Arce JL, Walker J, Keppie JD (2015) Petrology and geochemistry of El Chichón and Tacaná: two active, yet contrasting Mexican Volcanoes. In: Scolamacchia T, Macías JL (eds) Active Volcanoes of Chiapas (México): El Chichón and Tacaná. Springer, Berlin, pp 1–24. https://doi.org/10.1007/978-3-642-25890-9_1

    Chapter  Google Scholar 

  • Arellano-Contreras U, Jiménez-Salgado E (2012) Evaluación geológico-estructural del complejo volcánico Chichonal, Chiapas, como fuente alterna de energía. Geotermia, 3 p

  • Authemayou C, Brocard G, Teyssier C, Simon-Labric T, Gutiérrez A, Chiquín EN, Morán S (2011) The Caribbean-North America–Cocos triple junction and the dynamics of the Polochic-Motagua fault systems: pull-up and zipper models. Tectonics 30:1–23

    Article  Google Scholar 

  • Avellán DR, Macías JL, Layer PW, Sosa-Ceballos G, Gómez-Vasconcelos MG, Cisneros G, Sánchez-Núñez JM, Marti J, García-Tenorio F, López-Loera H, Pola A, Benowitz J (2019) Eruptive chronology of the Acoculco caldera complex—a resurgent caldera in the eastern Trans-Mexican Volcanic Belt (México). J S Am Earth Sci. https://doi.org/10.1016/j.jsames.2019.102412

    Article  Google Scholar 

  • Báez-Jorge F (1985) Cuando el cielo ardió y se quemó la tierra. Instituto Nacional Indigenista, México. p 158. ISBN 9688220558

  • Baranov V, Naudy H (1964) Numerical calculation of the formula of reduction to the magnetic pole. Geophysics 29:67–79

    Article  Google Scholar 

  • Blakely RJ (1996) Potential theory in gravity and magnetic applications. Cambridge University Press, Cambridge

    Google Scholar 

  • Bott MHP, Tantrigoda DA (1987) Interpretation of the gravity and magnetic anomalies over The Mull Tertiary Intrusive Complex, NW Scotland. J Geol Soc Lond 144:17–28

    Article  Google Scholar 

  • Bower SM, Woods AW (1998) On the influence of magma chambers in controlling the evolution of explosive volcanic eruptions. J Volcanol Geotherm Res 86:67–78. https://doi.org/10.1016/S0377-0273(98)00081-X

    Article  Google Scholar 

  • Brueseke ME, Hart W (2009) Intermediate composition magma production magma in an intracontinental setting: unusual andesites and dacites of the mid-Miocene Santa Rosa-Calico volcanic field, Northern Nevada. J Volcanol Geotherm Res 188:197–213

    Article  Google Scholar 

  • Burkart B (1983) Neogene North American-Caribbean plate boundary across Northern Central America: offset along the Polochic fault. Tectonophysics 99:251–270

    Article  Google Scholar 

  • Carrera-Muñoz M (2010) Geoquímica y petrología del arco volcánico chiapaneco (AVC) porción norte, Chiapas, México. Tesis de Maestría en el posgrado de Ciencias de la Tierra, UNAM, 112 p

  • Canul R, Rocha VL (1981) Informe geológico de la zona geotérmica de “El Chichonal” Chiapas. CFE, Morelia, p 38

    Google Scholar 

  • Canul R, Razo A, Rocha V (1983) Geología e historia vulcanológica del Volcán Chichonal. Instituto de Geología, UNAM, Ciudad de México, pp 9–22

    Google Scholar 

  • Capaul WA (1987) Volcanoes in the Chiapas Volcanic Belt, Mexico. M. Sc. Thesis, Michigan Technological University, Michigan

  • Carfantan JC (1976) El prolongamiento del sistema de fallas Polochic-Motagua en el sureste de México; una frontera entre dos provincias geológicas. Abstract III. Congreso Latino Americano de Geología, Acapulco, México

  • Couch R, Woodcock S (1981) Gravity and structure of the continental margins of southwestern Mexico and northwestern Guatemala. J Geophys Res 86:1829–1840

    Article  Google Scholar 

  • Damon P, Montesinos E (1978) Late Cenozoic volcanism and metallogenesis over an active Benioff Zone in Chiapas, Mexico. Ariz Geol Soc Dig 11:155–168

    Google Scholar 

  • De la Cruz-Reyna S, Martin del Pozzo AL (2009) The 1982 eruption of El Chichón Volcano, Mexico: eye–witness perspectives of the disaster. Geofís Int 48(1):12–31

    Google Scholar 

  • DeMets C (2001) A new estimate for present-day Cocos-Caribbean plate and Implications for slip along the Central American volcanic arc. Geophys Res Lett 28:4043–4046

    Article  Google Scholar 

  • Duffield WA, Tilling RI, Canul R (1984) Geology of El Chichón volcano, Chiapas, Mexico. J Volcanol Geotherm Res 20:117–132

    Article  Google Scholar 

  • Ellis RG, Wet B, Macleod IN (2012) Inversion of magnetic data from remanent and induced sources, magnetization vector inversion of the Pirapora anomaly. In: Fourteenth international congress of the Brazilian geophysical society 6, 22nd international geophysical conference and exhibition, Australia

  • Espíndola JM, Macías JL, Tilling RI, Sheridan M (2000) Eruptive history of El Chichón volcano (Chiapas, Mexico) during the Holocene and its impact on human activity. Bull Volcanol 62:90–104

    Article  Google Scholar 

  • Espíndola JM, Macías JL, Godínez L, Jiménez Z (2002) La erupción de 1982 del Volcán Chichónal, Chiapas, México. In: Lugo HJ, Inbar M (eds) Desastres naturales en América Latina. D. F., Fondo de Cultura Económica, México, pp 37–65

    Google Scholar 

  • Espíndola VH, Quintanar L, Espíndola JM (2016) Crustal structure beneath Mexico from receiver functions. Bull Seismol Soc Am 107:2427–2442. https://doi.org/10.1785/0120160152

    Article  Google Scholar 

  • Fernández-Cordoba J, Zamora-Camacho A, Espíndola JM (2017) Gravity survey at the Ceboruco Volcano área (Nayarit, Mexico): a 3-D model of the subsurface structure. Pure appl Geophys 174:3905–3918. https://doi.org/10.1016/j.jvolgeores.2015.05.001

    Article  Google Scholar 

  • Franco A, Lasserre C, Lyon-Caen H, Kostoglodov V, Molina E, Guzman-Speziale M, Monterosso D, Robles V, Figueroa C, Amaya W, Barrier E, Chiquin L, Moran S (2012) Fault kinematics in northern Central America and coupling along the subduction interface of the Cocos Plate, from GPS data in Chiapas (Mexico), Guatemala and El Salvador. Geophys J Int 189:1223–1236

    Article  Google Scholar 

  • García-Abdeslem J, Calmus T (2015) A 3D model of crustal magnetization at the Pinacate Volcanic Field, NW Sonora, Mexico. J Volcanol Geotherm Res 301:29–37. https://doi.org/10.1016/j.jvolgeores.2015.05.001

    Article  Google Scholar 

  • García-Palomo A, Macías JL, Espindola JM (2004) Strike-slip faults and K-alkaline volcanism at El Chichón volcano, southeastern Mexico. J Volcanol Geotherm Res 136:247–268

    Article  Google Scholar 

  • Garduño-Monroy VH, Macías JL, Molina R (2015) Geodynamic setting and pre-volcanic geology of active volcanism in Chiapas. In: Scolamacchia T, Macías JL (eds) Active volcanoes of Chiapas (México): El Chichón and Tacaná. Springer, Berlin, pp 1–24. https://doi.org/10.1007/978-3-642-25890-9_1

    Chapter  Google Scholar 

  • Guzmán-Speziale M (2001) Active seismic deformation in the grabens of northern Central America and its relationship to the relative motion of the North American-Caribbean plate boundary. Tectonophysics 337:39–51

    Article  Google Scholar 

  • Guzmán-Speziale M, Meneses-Rocha JJ (2000) The North America-Caribbean plate boundary best of the Motagua-Polochic fault system: a fault jog in Southeastern Mexico. J S Am Earth Sci 13:459–468

    Article  Google Scholar 

  • Guzmán-Speziale M, Pennington WD, Matumoto T (1989) The triple junction of the North America, Cocos, and Caribbean Plates: seismicity and tectonics. Tectonics 8:981–999

    Article  Google Scholar 

  • Hamelin B, Manhes G, Albarede F, Allegre CJ (1985) Precise lead isotope measurements by the double spike technique: a reconsideration. Geochim Cosmochim Acta 49:173–182

    Article  Google Scholar 

  • Henderson RG, Zietz I (1949a) The upward continuation of anomalies in total magnetic intensity fields. Geophysics 14:517–534

    Article  Google Scholar 

  • Henderson RG, Zietz I (1949b) The computation of second vertical derivatives of geomagnetic fields. Geophysics 14:508–516

    Article  Google Scholar 

  • Hildreth W, Moorbath S (1988) Crustal contributions to arc magmatism in the Andes of central Chile. Contrib Mineral Pet 98:455–489

    Article  Google Scholar 

  • House T, McMahon TP (2000) Ancient isotopic characteristics of Neogene potassic magmatism in western New Guinea (Irian Jaya, Indonesia). Lithos 50:217–239

    Article  Google Scholar 

  • Hunt CP, Moskowitz Bruce M, Banerje SK (1995) Magnetic properties of rocks and minerals. In: Ahrens TJ (ed) Rock physics and phase relations: a handbook of physical constants. American Geophysical Union Reference Shelf, Washington, DC, p 31

    Google Scholar 

  • IGRF (2000) International geomagnetic reference field. IAGA. Division V-Mod, Geomagnetic field modeling

  • IGRF (2005) International geomagnetic reference field. IAGA. Division V-Mod, Geomagnetic Field Modeling

  • INEGI (2005) Instituto Nacional de Estadística y Geografía. https://www.inegi.org.mx/app/mapas/

  • Jansen NH (2012) Geology and genesis of the Cerro la Mina porphyry-high sulfidation prospect, Unpublished PhD thesis. University of Tasmania, Mexico, Australia, 222 p

  • Jansen HN, Gemmell BJ, Chang Z, Cooke RD, Jourdan F, Creaser AR, Hollings P (2017) Geology and genesis of the Cerro la Mina Porphyry-high sulfidation Au (Cu-Mo) prospect, Mexico. Econ Geol 112(4):799–827

    Article  Google Scholar 

  • Jaimes-Viera MC (2006) Petrología y Geoquímica del Arco Volcánico Chiapaneco. Tesis de Maestría en el posgrado de Ciencias de la Tierra, UNAM, 138 p

  • Jiménez Z, Espíndola VH, Espíndola JM (1999) Evolution of the seismic activity from the 1982 eruption of El Chichon Volcano, Chiapas, Mexico. Bull Volcanol 61:41122

    Article  Google Scholar 

  • Jutzeler M, Varley N, Roach M (2011) Geophysical characterization of hydrothermal systems and intrusive bodies, El Chichón volcano (Mexico). J Geophys Res 116:B04104

    Article  Google Scholar 

  • Lassiter JC, Blichert-Toft J, Hauri EH, Barsczus HG (2003) Isotope and trace element variations in lavas from Raivavae and Rapa, Cook Austral islands: constraints on the nature of HIMU- and EM-mantle and the origin of mid-plate volcanism in French Polynesia. Chem Geol 202:115–138

    Article  Google Scholar 

  • Layer PW (2000) Argon-40/argon-39 age of the El’gygytgyn impact event, Chukotka, Russia. Meteorit Planet Sci 35:591–599

    Article  Google Scholar 

  • Layer PW, García-Palomo A, Jones D, Macias JL, Arce JL, Mora JC (2009) El Chichón Volcanic Complex, Chiapas, Mexico: stages of evolution based on field mapping and 40Ar/39Ar geochronology. Geofís Int 48(1):33–54

    Google Scholar 

  • Le Bas MJ, Le Maitre RW, Streckaisen A, Zanettin B (1986) A chemical classification of volcanic rocks based on the total alkali-silica diagram. J Petrol 27:745–750

    Article  Google Scholar 

  • Le Fevre LV, McNally KC (1985) Stress distribution and subduction of aseismic ridges in the middle America Subduction Zone. Geophys Res Lett 90(B6):4495–4510

    Article  Google Scholar 

  • Li Y, Oldenburg DW (1996) 3-D inversion of magnetic data. Geophysics 61:394–408. https://doi.org/10.1190/1.1443968

    Article  Google Scholar 

  • López-Loera H (2002) Estudio de las Anomalías Magnéticas y su relación con las Estructuras Geológicas y Actividad Eruptiva de los Complejos Volcánicos Activos de Colima e Izta-Popocatepetl, México. Tesis Doctoral, Instituto de Geofísica, UNAM, p 296

  • López-Loera H, Urrutia-Fucugachi J, Alva-Valdivia L (2011) Estudio aeromagnético del complejo volcánico de Colima, occidente de México – implicaciones tectónicas y estructurales. Rev Mex Cienc Geol 28(3):349–370

    Google Scholar 

  • Lozano-Santacruz R, Bernal JP (2005) Characterization of a new set of eight geochemical reference materials for XRF major and trace element analysis. Rev Mex Cienc Geol 22:329–344

    Google Scholar 

  • Luhr JF, Carmichael ISE, Varekamp JC (1984) The 1982 eruptions of El Chichón Volcano, Chiapas, Mexico: mineralogy and petrology of the anhydrite–bearing pumice. J Volcanol Geotherm Res 23:69–108

    Article  Google Scholar 

  • Macías JL, Arce JL, Mora JC, Espíndola JM, Saucedo R, Manetti P (2003) A 550 years old Plinian eruption at El Chichón volcano, Chiapas, Mexico: explosive volcanism linked to reheating of the magma reservoir. J Geophys Res 108(B12):2569

    Article  Google Scholar 

  • Macías JL, Arce JL, Garduño-Monroy VH, Rouwet D, Taran Y, Layer PW, Jiménez A, Álvarez R (2010) Estudio de prospección geotérmica para evaluar el potencial del volcán Chichonal, Chiapas. Unpublished report no. 9400047770 IGF-UNAM-CFE

  • Manea V, Manea M (2006) Origin of the modern Chiapanecan Volcanic arc in southern Mexico inferred from thermal models. GSA Spec Pap 412:27–38

    Google Scholar 

  • Manea M, Manea VC (2008) On the origin of El Chichón volcano and subduction of Tehuantepec Ridge: a geodynamical perspective. J Volcanol Geotherm Res 175(4):459–492. https://doi.org/10.1016/j.jvolgeores.2008.02.028

    Article  Google Scholar 

  • Marsh BD (2015) Magma chambers. In: Sigurdsson H, Houghton B, McNutt S, Rymer H, Stix J (eds) Encyclopedia of volcanoes. Academic Press, Cambrdige. ISBN 9780123859389

    Chapter  Google Scholar 

  • Mazot A, Rouwet D, Taran Y, Inguaggiato S, Varley NR (2011) CO2 and He degassing at El Chichón volcano, Chiapas, Mexico: Gas flux, origin, and relationship with local and regional tectonics. Bull Volcanol. https://doi.org/10.1007/s00445-010-0443-y

    Article  Google Scholar 

  • McDougall I, Harrison TM (1999) Geochronology and thermochronology by the 40Ar/39Ar method, 2nd edn. Oxford University Press, New York, p 269

    Google Scholar 

  • McNulty BA, Tobish OT, Cruden AR, Gilder S (2000) Multi-stage emplacement of the Mount Givens pluton, central Sierra Nevada batholith, California. Geol Soc Am Bull 112(1):119–135

    Article  Google Scholar 

  • Meneses-Rocha JJ (1985) Tectonic evolution of the Strike-slip Fault province of Chiapas. Mexico [MS thesis]: Austin, Texas, University of Texas at Austi, 315 p

  • Meneses-Rocha JJ (2001) Tectonic evolution of the Ixtapa Graben, an example of a strike-slip basin of southeastern Mexico: implications for regional petroleum systems. In: Bartolini C, Buffler RT, Cantú-Chapa A (eds) The western Gulf of Mexico Basin: tectonics, sedimentary basins, and petroleum systems. AAPG. Mem. 75. AAPG, Tulsa, p 75

    Google Scholar 

  • Molina-Garza RS, Geissman JW, Wawrzyniec TF, Peña Alonso TA, Iriondo A, Weber B, Aranda-Gómez J (2015) Geology of the coastal Chiapas (Mexico) Miocene plutons and the Tonalá shear zone: syntectonic emplacement and rapid exhumation during sinistral transpression. Lithosphere 7(3):257–274

    Article  Google Scholar 

  • Mora JC, Jaimes-Viera MC, Garduño-Monroy VH, Layer PW, Pompa-Mera V, Godinez ML (2007) Geology and geochemistry characteristics of the Chiapanecan Volcanic Arc (Central Area), Chiapas Mexico. J Volcanol Geotherm Res 162:43–72

    Article  Google Scholar 

  • Mora JC, Layer PW, Jaimes-Viera MC (2012) New 40Ar/39Ar ages from the Central Part of the Chiapanecan Volcanic Arc, Chiapas, Mexico. Geofis Int 51:39–49

    Google Scholar 

  • Mori L, Gómez-Tuena A, Cai Y, Goldstein SL (2007) Effects of prolonged flat subduction on the Miocene magmatic record of the central Trans-Mexican Volcanic Belt: chemical geology: including isotope. Geoscience 244:452–473

    Google Scholar 

  • Mülliered FKG (1933) “El Volcán”, único volcán en actividad descubierto en el estado de Chiapas. Mem Rev Acad Ciencias “Antonio Alzate” 5(11/12):411–416

    Google Scholar 

  • Nabighian MN (1972) The analytic signal of two-dimensional magnetic bodies with polygonal cross-section: its properties and use for automated anomaly interpretation. Geophysics 37(3):507–517

    Article  Google Scholar 

  • Nabighian MN (1974) Additional comments on the analytic signal of two-dimensional magnetic bodies with a polygonal cross-section. Geophys 39(1):85–92

    Article  Google Scholar 

  • Nixon GT (1982) The relationship between Quaternary volcanism in central Mexico and the seismicity and structure of the subducted ocean lithosphere. Geol Soc Am Bull 93:514–523

    Article  Google Scholar 

  • Pardo M, Suárez G (1995) Shape of the subducted Rivera and Cocos plates in southern Mexico: seismic and tectonic implications. J Geophys Res 100:12357–12373

    Article  Google Scholar 

  • Pindell J, Kennan L, Maresch WV, Stanek KP, Draper G, Higgs R (2005) Plate-kinematics and crustal dynamics of circum-Caribbean arc continent interactions. In: Avé‐ Lallemant HG, Sisson VB (eds) Tectonic controls on basin development in Proto-Caribbean Margins. Special Papers—Geological Society of America, vol 394, pp 7–52

  • Ratschbacher L, Franz L, Min M, Bachmann R, Martens U, Stanek K, Stübner K, Nelson BK, Herrmann U, Weber B, López-Martínez M, Jonckheere R, Sperner B, Tichomirowa M, Mcwilliams MO, Gordon M, Meschede M, Bock P (2009) The North American-Caribbean plate boundary in Mexico-Guatemala-Honduras. In: Martini IP, French HM, Pérez-Alberti A (eds) Ice-marginal and periglacial processes and sediments, vol 328. Geological Society London Special Publications, London, pp 219–293. https://doi.org/10.1144/sp328.11

    Chapter  Google Scholar 

  • Rebollar CJ, Espíndola VH, Uribe A, Mendoza A, Pérez-Vertti A (1999) Distribution of stress and geometry of the Wadati-Benioff zone under Chiapas, Mexico. Geofís Int 38:95–106

    Google Scholar 

  • Renne PR, Mundil R, Balco G, Min K, Ludwig K (2010) Joint determination of 40 K decay constants and the 40Ar*/40K for the Fish Canyon sanidine standard and improved accuracy for 40Ar/39Ar geochronology. Geochim Cosmochim Acta 74:5349–5367

    Article  Google Scholar 

  • Sawires R, Aboud E (2019) Subsurface structural imaging of Ceboruco Volcano area, Nayarit, Mexico using high-resolution aeromagnetic data. J Volcanol Geotherm Res 371:162–176. https://doi.org/10.1016/j.jvolgeores.2019.01.012

    Article  Google Scholar 

  • Scolamacchia T, Capra L (2015) El Chichón Volcano: Eruptive History. In: Scolamacchia T, Macías JL (eds) Active Volcanoes of Chiapas (México): El Chichón and Tacaná. Springer, Berlin, pp 45–76. https://doi.org/10.1007/978-3-642-25890-9_1

    Chapter  Google Scholar 

  • Scolamacchia T, Macías JL (2015) Active Volcanoes of Chiapas (México): El Chichón and Tacaná. Active Volcanoes of the world. Springer, April. ISSN 2195-3589. https://doi.org/10.1007/978-3-642-25890-9

    Google Scholar 

  • Servicio Geológico Mexicano (1996) Carta Geológico Minera Villahermosa E15-8 Tab., Ver., Chis., Oax. 2nd Edition. Chart

  • Spector A, Grant FS (1970) Statistical models for interpreting aeromagnetic data. Geophysics 35(2):293–302

    Article  Google Scholar 

  • Steiger RH, Jaeger E (1977) Subcommission on geochronology: convention on the use of decay constants in geo and cosmochronology. Earth Planet Sci Lett 36:359–362

    Article  Google Scholar 

  • Sulpizio R, Zanella E, Macías JL (2008) Deposition temperature of some PDC deposits from the 1982 eruption of El Chichón volcano (Chiapas, Mexico) inferred from rock-magnetic data. J Volcanol Geotherm Res 175:494–500

    Article  Google Scholar 

  • Sun S, McDonough W (1989) Chemical and isotopic systematics of oceanic basalts: implications for mantle compositions and processes. In: Saunders A, Norry M (eds) Magmatism in ocean basins, vol 42. Geological Society London Special Publications, Burlington House, pp 313–345

    Google Scholar 

  • Tikhonov AN (1963) Solution of incorrectly formulated problems and the regularization method, Soviet Math Dokl 4:1035–1038 (English translation of Dokl Akad Nauk SSSR 151: 501–504)

  • Tilling RI (2009) El Chichón’s “surprise” eruption in 1982: lessons for reducing volcano risk. Geofís Int 48:3–19

    Google Scholar 

  • Truchan M, Larson RL (1973) Tectonic lineaments on the Cocos plate. Earth Planet Sci Lett 17:426–432. https://doi.org/10.1016/0012-821X(73)90211-2

    Article  Google Scholar 

  • Verma PS, Verma KS (2018) Petrogenetic and tectonic implications of major and trace element and radiogenic isotope geochemistry of Pliocene to Holocene rocks from the Tacaná Volcanic Complex and Chiapanecan Volcanic Belt, southern Mexico. Lithos 312–313:274–289

    Article  Google Scholar 

  • Wawrzyniec T, Molina-Garza RS, Geissman JW, Iriondo A (2005) A newly discovered relic, transcurrent plate boundary—the Tonalá shear zone and paleomagnetic evaluation of the western Maya block, S.W. Mexico. Geol Soc Am Abstr Prog 37:68

    Google Scholar 

  • Zuñiga FR, Díaz LE (1994) Coda attenuation in the area of El Chichón volcano, Chiapas, Mexico. Tectonophysics 234:247–258

    Article  Google Scholar 

Download references

Acknowledgements

We thank F. García for his technical support during the laboratory analyses and G. Cisneros for his support during image processing and some map generation. We are also grateful to Dr. Robert I. Tilling and two anonymous reviewers for their constructive comments, which greatly improved the original manuscript.

Author information

Authors and Affiliations

  1. Geociencias Aplicadas, Instituto Potosino de Investigación Científica y Tecnológica A.C., Camino a la Presa de San José 2055, Lomas 4a sección, 78216, San Luis Potosí, S.L.P, Mexico

    Héctor López-Loera & David Ernesto Torres-Gaytan

  2. Instituto de Geofísica, Unidad Michoacán, Universidad Nacional Autónoma de México, Campus Morelia, Antigua Carretera a Pátzcuaro 8701, 58059, Morelia, Michoacán, Mexico

    José Luis Macías

  3. Instituto de Geofísica, Universidad Nacional Autónoma de México, Av. Universidad 3000, Coyoacán, 04510, Mexico City, Mexico

    Juan Manuel Espíndola

  4. Instituto de Geología, Universidad Nacional Autónoma de México, Av. Universidad 3000, Coyoacán, 04510, Mexico City, Mexico

    José Luis Arce

  5. College of Natural Science, Mathematics and Geophysical Institute, University of Alaska at Fairbanks, Fairbanks, AK, 99775, USA

    Paul W. Layer

Authors
  1. Héctor López-Loera
    View author publications

    You can also search for this author in PubMed Google Scholar

  2. José Luis Macías
    View author publications

    You can also search for this author in PubMed Google Scholar

  3. Juan Manuel Espíndola
    View author publications

    You can also search for this author in PubMed Google Scholar

  4. José Luis Arce
    View author publications

    You can also search for this author in PubMed Google Scholar

  5. Paul W. Layer
    View author publications

    You can also search for this author in PubMed Google Scholar

  6. David Ernesto Torres-Gaytan
    View author publications

    You can also search for this author in PubMed Google Scholar

Corresponding author

Correspondence to Héctor López-Loera.

Additional information

Publisher's Note

Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Appendices

Appendix 1

1.1 Whole-Rock Geochemical Analysis

We collected three samples from structures that to our knowledge had not been analyzed before. One of the samples was collected from an intrusive body (MCH516) that correlates with rocks of the Santa Fe mining district described by Damon and Montesinos (1978), which are defined here as Santa Fe Intrusive. The second sample is a block (MCH505B) from the Catedral volcanoclastic fan, and the third is a mafic enclave (CH0902E) hosted in an andesitic block of El Chichón volcano. These three samples were collected for petrographic and geochemical analysis and 40Ar/39Ar dating.

1.2 X-Ray Fluorescence (XRF) Analysis

The XRF analyses of major and some trace elements (Rb, Sr, Ba, Y, Zr, Nb, V, Cr, Co, Ni, Cu, Zn, Th, and Pb) have precisions of < 1% for all elements (Table 1). These analyses were carried out at the Laboratorio Nacional de Geoquímica y Mineralogía, UNAM, México, following the methodology described in Lozano-Santacruz and Bernal (2005). Trace elements were determined by inductively coupled plasma mass spectrometry, at the Laboratorio de Estudios Isotópicos (LEI) UNAM, using a Thermo Series XII spectrometer, following Mori et al. (2007).

1.3 Sr, Nd, and Pb Isotopic Analysis

The Sr, Nd, and Pb isotopic analyses of selected samples were carried out at the Jackson School of Geosciences, University of Texas at Austin, USA, using a Thermo Triton TI thermal ionization mass spectrometer (TIMS), following standard procedures on whole-rock chips (Table 1). Groundmass chips that lacked visible alteration or phenocrysts were handpicked under a binocular microscope. Chips were first leached in hot 6 N HCl to remove any caliche or weathered material and then digested in HF:HNO3. Sr, Nd, and Pb were extracted and purified following standard procedures after Lassiter et al. (2003). Sr-Spec, REE-spec/HDEHP, and AG1-X8 resins were used to separate Sr, Nd, and Pb, respectively.

Measurements were carried out in manual and programme modes and included two total procedural blanks and two sample duplicate analyses. Sr was loaded on single Re filaments with Ta2O5; mass fractionation of 87Sr/86Sr ratios was corrected using 88Sr/86Sr = 8.375209. Neodymium was run as metal on double Re filaments. 143Nd/144Nd ratios were corrected for mass fractionation using 146Nd/144Nd = 0.7219. During the course of this study, 32 analyses of Sr standard NBS 987 yielded a value of 0.710263 ± 9 (2σ). An in-house UT Ames Nd standard yielded a 143Nd/144Nd = 0.512069 ± 6 (2σ). Pb-isotope analyses were corrected for mass fractionation using a double-spike technique modified from Hamelin et al. (1985), House and McMahon (2000). Seven double-spiked fractionation corrected NBS 981 analysis carried out in this study yielded mean Pb isotopic ratios of:

$$\begin{aligned}^{206} {\text{Pb}}/^{204} {\text{Pb}}\, = \,16.9336 \, \pm \, 0.0048 \hfill \\^{207} {\text{Pb}}/^{204} {\text{Pb}}\, = \,15.4887 \, \pm \, 0.0063 \hfill \\^{208} {\text{Pb}}/^{204} {\text{Pb}}\, = \,36.6907 \, \pm \, 0.0207 \hfill \\ \end{aligned}$$

1.4 40Ar/39Ar Analysis

The samples were dated with the 40Ar/39Ar method used at the University of Alaska Fairbanks geochronology laboratory by laser step-heating of phenocryst-free groundmass chips (1 to 0.5 mm size fraction) following the procedures outlined in Layer (2000) and Layer et al. (2009). The mineral TCR-2 with an age of 28.6 Ma (Renne et al. 2010) was used to monitor neutron flux and calculate the irradiation parameter, J, for all samples. The measured argon isotopes were corrected for system blank and mass discrimination, and for the irradiated samples, calcium, potassium, and chlorine interference reactions, following the procedures of McDougall and Harrison (1999). Ages were calculated using the constants of Renne et al. (2010) and are reported at the 1-sigma level. Typical full-system, fifteen-minute laser blank values (in moles) were generally 6 × 10–16 mol 40Ar, 3 × 10–18 mol 39Ar, 3 × 10–18 mol 38Ar and 1 × 10–17 mol 36Ar, which are 10 to 50 times smaller than the sample/standard volume fractions. Mass discrimination was monitored by running calibrated air shots. The mass discrimination during this method was 1.0% per mass unit. Two runs of each sample were done, and the most precise run was chosen for presentation and discussion. A sample is considered to have defined a plateau age if it has 3 or more contiguous fractions constituting at least 50% 39Ar release and is significant at the 95% confidence level (as indicated by a Mean Square Weighted Deviates; MSWD < ~ 2.5). For the two samples analyzed, plateau ages yielded the most interpretable results due to little isotopic variation between the steps. The results are quoted to the ± 1 sigma level and calculated using the constants of Steiger and Jaeger (1977). The results are given in Table 2.

Appendix 2

Detailed information and attributes of the eight aeromagnetic domains (AMDs) recognized from this study in the RPMF (Fig. 7a); additional information is given in Table 4.

AMD I This domain is located in the central portion of the study zone and is characterized by a dipolar anomaly of large extent spanning, ~ 52 km in the N–S direction and ~ 40 km in the E–W direction. The magnetic high is elongated in the NNE–SSW direction with a length of ~ 27 km and ~ 24 km in the E–W direction. The magnetic low runs for ~ 37 km along the E–W direction and is ~ 19 km in the N–S direction. The anomaly is associated with a large granodioritic-dioritic intrusion cropping out around the central portion of the anomaly. In the surrounding areas, the anomaly is associated with sedimentary rocks, mostly intercalations limestone-sandstone and limonite-limestone, except to the west where it is associated with andesite breccias and andesites from the El Chichón volcano complex.

AMD II comprises the area to the north, where it meets the edge of the study area, and diffuses into nearby areas of smaller magnetic field intensity, which we labeled as domains IIa and IIb.

AMD II is characterized by its large size (~ 152 km in the E–W direction and ~ 78 km in the N–S) and seems to be associated with a magnetic high toward the N, beyond the study area. The anomaly has a somewhat slant L-shaped form. The magnetic high has gradients that increase at a rate of 0.00257 nT/m from S to N, 0.0051 nT/m from the west to the center, and 0.00078 nT/m from the center to the east. The topography in this area varies from 619 masl to the S to 25.5 masl to the N. It correlates with shale-limestone to the center and west, with shales-sandstones to the S, sandstone-polymictic conglomerates to the N, and alluvium and andesitic breccias to the E.

AMD IIa is found south of AMD II, it is elongated in an NW–SE trend measuring approximately 54 km, and 30 km in the NE–SW direction. Its magnetic intensity shows values between − 163 nT and − 112 nT, with an average of − 129 nT. Its topography varies from 230 1273 masl, with an average of 339 masl, and 230 masl toward the NW to the center, after that increasing to reach 1273 masl at the center and 552 masl to the SE. Geologically, it correlates with limestones-shales, limestones-dolomites, alluvium, and limonite-sandstone around the center.

AMD IIb lies to the east of AMD II and is characterized by similar magnetic field intensity to AMD IIa, with a gradient of only 0.00068 nT/m. It has an irregular elongated shape toward the S, and narrows toward the N. It is geologically associated with limestone-sandstones to the S and sandstones-shales to the N. The topography increases from 5 masl to the north to 189 to the south, but it reaches an altitude of about of 665 masl somewhere between the center and the south.

AMD III is located to the E and SE of AMD I and extends for 86 km to the NW–SE. A minor axis oriented NW–SE has a length of about 33 km. Magnetically it shows low values ranging from − 266 to − 206 nT, with a mean value of − 224 nT. Geologically, most of the domain correlates sandstones-shales and outcropping shales-limestones. The altitudes in the domain vary from 281 to 1882 masl to the SE, 1288 masl to the NW (where it meets AMDI) and 281 masl in the center.

AMD IV is a domain defined in three separated zones, two of them neighboring AMD III. They are banded with the long axis striking roughly NW–SE. The three sections are described in the following sub-domains.

AMD IVa comprises the south-center of the area, with a length of 41 km and a width of 23 km in the NE–SW direction. Magnetically, it shows a discrete gradient from NE to SW, going from − 200 to − 158 nT, with a variation of 0.0019 nT/m. It is associated with dolomites and alluvium. Topographically, it varies from 119 to 2073 masl, with an average of 1545 masl, the lowest values in the central portion and the highest in the NE.

AMD IVb is located in the NE portion of the zone, in the vicinity of AMD IIb and III. It has a length of the order of 68 km and 23 km in the perpendicular direction. Toward the NW portion, in the limits with the AMD II, it shows some small anomalies with magnetization intensities averaging 7.4 nT (157.3 to 164.7 nT) with a horizontal gradient of 0.0064 nT/m, and 12.8 nT (156.9 to 169.7 nT) with a horizontal gradient of 0.010 nT/m, respectively. In the NW–SE direction the domain presents magnetization intensity values ranging from − 186.3 to − 127.3 nT, with an average of − 172.4 nT. With the exception of the NW portion, where the small anomalies appear, the section shows two groups of intensities: one toward the NW central portion with values from − 169.2 to − 156.7 nT (with altitudes ranging from 1151 to 929 masl), and another from the center to the SE with values of − 183 to − 164.4 nT and a gradient of 0.0005 nT/m. Topographically, it exhibits two morphologies: one in the NW portion, running from 11.5 to 190.7 masl, and another one from the center to the NE going from 1158 to 1595 masl with an average of 1189 masl.

The NE–SW section of this domain presents magnetization intensities ranging from − 205 to − 140 nT, decreasing toward the NW and increasing to the NE, and a horizontal gradient of 0.00276 nT/m. The relief shows two morphologies, one from center to the NW of 272 masl to 1537 masl, with an average of 1032 masl, and another from center toward the NE from 272 to 34.3 m, with an average of 145 masl. The surface rocks are fundamentally shale-limestone, limestone-sandstone, and alluvium.

AMD IVc is defined by the SW portion of the study area and bounded by AMDs II and IIa to the NE and E, respectively, by AMD VII to the SW, and by AMD VIII to the NW. It is elongated, inclined toward the NW and consists of a long and wide section and two branches, one trending roughly N–S, and the second to the west. Its dimensions are 77.5 km in the NW–SE direction, up to the intersection of the two branches. At about 3.3 km from the intersection, the N–S branch has a width of 6.8 km in the NE–SW direction. The west branch has a length of 12.3 km and a width of 3.9 km.

The long section of the domain presents variations in the intensity of magnetization ranging from − 212 to − 163.7 nT and a horizontal gradient of 0.00062 nT/m. The topography varies from 152 masl to the NW to 1239 masl to the SE. The intensity of magnetization in the N–S branch range from − 205 (SSE) to − 157.7 nT (NNW), with an average of − 176.4 nT. The topography varies from 6 to 416 masl from the NNW to the SSE. The western branch spans 10 km and ranges in its magnetization intensity from − 190 to − 181 nT. Topographically, it has heights of 770 to 965 masl, which increase toward the west.

AMD V is located near the SE, in the vicinity of AMDs III, IVa and VI. It is cut off to the S by the limit of the study area and is characterized by a series of magnetic anomalies with a preponderance of magnetic lows. It has an amorphous shape, although somewhat elongated in the north direction with a length of 31.6 km. In the E–W direction, it varies from 36 km in the southern part to 20 km in the northern portion.

The anomalies have different intensities of magnetization; one shows an amplitude of 175.4 nT (varying from − 119.6 to − 295 nT) with a polar distance of 395 m. A second one has an intensity of 221.4 nT (− 130.1 to − 351.5 nT) with a polar distance of 5300 m. The topography changes from 1356 to 2383 masl from the SW to the NE. Geologically, the domain is associated with limestones-shales, and limonites-sandstones; the anomalies, however, are correlated with andesitic tuffs.

AMD VI is located in the southern part of the area and is incomplete as it is cut by the edge of the study area. It is elongated with a length of 21 km in NW–SE direction, and 10.7 km, wide. Magnetically it is a monopole with a magnetic high of 134 nT (− 158.6 nT at − 24.7 nT). The magnetic intensity in the domain ranges from − 180.1 to − 24.7 nT. In the domain it is possible to observe part of another monopole, showing values up to 63 nT. The terrain presents heights going from 1049 to 1908 masl, increasing in intensity from NW to SE. The domain is associated with andesites-andesitic tuffs. The monopoles are interpreted as due to protuberances on an intrusion of basic to intermediate composition.

AMD VII is identified in the SW corner of the study area and is cut both to the south and west. It is elongated with a length of 57.4 km in the NW–SE direction and 40 km in the NE–SW direction. At the center and south part, it contains a succession of small anomalies resembling a stone pavement showing various magnetization amplitudes ranging from − 175.4 to − 6.8 nT. Individual intensities are: 15.2 nT (− 6.8 to 22 nT), 56.1 nT (− 119.3 to − 175.4 nT), 85.5 nT (− 17.7 to − 103.2 nT) with a polar distance of 1.7 km. The highs are aligned in an NW–SE direction. Altitudes in the area range from 353 to 1256 masl.

A profile in an NE–SW direction reveals a series of small anomalies with magnetization intensities of 204.1 nT (− 16.2 to − 220.3 nT) and a polar distance of 3.4 km. The magnetic low is associated with a lineament in the NW–SE direction. Other magnetic anomalies have amplitudes of the order of 59.7 nT (− 63.8 to − 123.5 nT) with a polar distance of 1.45 km and 17.2 nT (− 102.9 to − 120.1 nT). The zone of magnetic lows has an NW–SE trend and is associated with zones of weakness, faults and (or) fractures. Topographically, the altitude varies from 319 to 1397 masl, from NE to SW. The area contains andesitic breccias and tuffs to the SW, and limestones and dolomites to the NE.

AMD VIII is located toward the NW end of the study zone, where it is cut off by its north and west margins. It is elongated with a length of 63 km in the NNW-SSE direction and an average width of 13.4 km. The entire domain is characterized by values associated with magnetic lows shown in three subdomains. One is located in the NNW portion with values from − 255 to − 226 nT, averaging − 232 nT. It correlates topographically with values going from 6 to 89 masl, from NW to SE. The second subdomain with magnetization intensities from − 284 to − 252 nT can be identified in the central portion of the domain. Topographically, it ranges from 40 to 419 masl. A third subdomain reckons magnetization intensity values between − 263 and − 210 nT, with a horizontal gradient increasing to the SW of 0.0041 nT/m. Topographically, it varies from 209 to 828 masl, rising toward the SE. The domain is geologically associated mostly with shale and limestone-dolomite.

Appendix 3

Detailed information and attributes of the seven aeromagnetic domains (AMDs) recognized from the study of the 2nd Derivative in Z direction; additional information given in Table 5.

AMD I is located mostly in the central portion of the study area, it is elongated with an average length of 31 km in the N–S direction, and 20 km in length to the E–W direction. It encloses a magnetic high surrounded, except to the west limit, by magnetic lows (− 0.00255 × 10−2 to − 0.000742 × 10−2 nT). On the surface, it is associated with limestones-sandstones, and a small outcrop of intrusive granodiorite-diorite, which suggests the presence of a sizeable granodioritic body below.

AMD II comprises a good part of the study area. Its main location is somewhat west of the center and its shape is amorphous, formed by a series of magnetic highs and lows aligned in such a way that a preferential direction cannot be distinguished. Toward the W, the dominant direction is NW–SE; at the center and the NE the direction is E–W, and toward the S the direction is N–S. This series of magnetic highs and lows have wavelengths spanning from 1850 to 4100 m. The magnetic intensity values fall in the interval from 0.013 × 10−2 to − 0.02 × 10−2 nT. El Chichón volcano is located in this domain. Geologically most of the surface rocks are shales and limestones, but there are also outcrops of andesitic breccia. For a better description this AMD was divided into the following subdomains:

AMD IIa is a section located to the north of the study area and limited by its edge. It is elongated, approximately 65 km along the E–W direction, and approximately 11 km wide. It is characterized by a sequence of highs and lows, mainly with an NE–SW and E–W trends. Their magnetic values oscillate between − 0.002 × 10−2 nT and 0.0037 × 10−2 nT; their wavelengths between 1900 and 2950 m with an average of about 2250 m. Most of this subdomain is covered by alluvium, with some outcrops of andesitic breccias.

AMD IIb is located in the SW corner of the study area and is cut off by the margins to the south and west. It has, therefore, a triangular shape with maximum dimensions of 51 km in the NW–SE direction and 27 km in the NE–SW. Magnetically it shows the same characteristics as AMD II. It is arranged in a series of consecutive highs and lows, with a preferential NW–SE trend, and wavelengths of the order of 2000 m. The magnetic values are in the range − 0.00217 × 10−2 nT and 0.0037 × 10−2 nT. The area is composed of breccias and andesitic tuffs.

AMD IIc is an elongated area situated toward the NW of the study area. With dimensions of 44 km to the NW–SE and 15 km to the NE–SW directions, it is cut off to the west by the study area´s edge. Magnetically, it is similar to other parts of the domain, consisting of stripes of magnetic highs and lows trending in the NW–SE direction. It shows magnetic values oscillating between − 0.00435 × 10−2 and 0.0023 × 10−2 nT, and terrain wavelengths of the order of 1800 m to 2, 325 m. The surface geology displays alluvium, sandstones-shales, shales-limestones and andesites-andesitic tuffs.

AMD III covers an almost square region to the east of the study area. Its dimensions are 73 km and 67 km in the in the E-W and N-S directions, respectively. Its shape is given by a series of banded highs trending NW–SE in a matrix of average values. The magnetic intensities vary between − 0.000430 × 10−2 nT and 0.000246 × 10−2 nT, and can be classified into three groups of different wavelengths, one of length 6.1 km topographically associated with elevations of 854 to 975 masl, another one of 7.9 nT with altitudes that go from 414 to 731 masl, and a third one of 9 km in length with height going from 1155 to 1336 masl. Most of the area of the domain contains sedimentary rocks: shales-limestones, limestones-sandstones, and limonites-sandstones. Around the center, however, there are mineral deposits.

AMD IV is composed of three sections: to the NW, NE and S of the study area, almost surrounding AMD II. These sections are cut off toward their NW, NE, E and S margins. It is characterized by showing a series of magnetic heights. The magnetic values range from − 0.00064 × 10−2 to 0.0013 × 10−2 nT in a setting of average values. There are high frequencies that can be classified into two groups: one with wavelengths from 1450 to 1550 m, another with wavelengths from 2050 to 2250 m. The NW portion of the domain has an area of 69 by 35 km in the E–W and N–S directions, respectively. The southern section is 40 km long in the N–S direction and 43 km along the E–W. The NE portion spans an area 35 km long along the N–S direction and 34 km along the E–W. Geologically, the NW part is associated with sandstones and polymictic conglomerates and shales-limestones. The NE part it is associated with limestones, sandstones, shales, and sandstones-limonites. The SW section is related to shales, limestones, and sandstones-shales.

AMD V is a somewhat elliptical domain is located in the SE, where it is cut off by the southern edge of the study area. Its dimensions are 61 and 2 km in the E–W and N–S directions, respectively. It is characterized by series of well-defined magnetic anomalies, showing evident bipolarity. Individual anomalies can be identified with values of 0.002988 × 10−2 nT and 0.001169 × 10−2 nT and polar distances of the order of 3.5 km. It contains wavelengths from 6450 to 7000 m. Geologically, it is associated with andesitic tuffs and sedimentary rocks, such as limestones, shales, and sandstones.

AMD VI is located toward the SW portion of the study area and is elongated with a long axis in the NW–SE direction, cut off in its extremes by the limits of the study area. It is 74 km in length along the NW–SE direction and, approximately 28 km wide. It shows bands of elongated magnetic highs of 34 km × 8.7 wide with values of up to 0.0006227 × 10−2 nT, embedded in a matrix with values ranging from − 0.00012 × 10−2 nT to − 0.00024 × 10−2 nT. It is related to limestones-dolomites, limestones-shales, and alluvium. See Table 2.

AMD VII is located toward the north central part of the studied área. It is limited to the W by AMD IV, to the E by AMD IIa and to the S by AMD II. It presents a shoe shape being elongated toward the W portion and in the NW–SE direction where it shows the dimensions of the order of the 26 km. See Table 2. Geologically it is correlates superficially with sandstones, polimictic conglomerate and with limestone-shale.

Rights and permissions

Reprints and permissions

About this article

Check for updates. Verify currency and authenticity via CrossMark

Cite this article

López-Loera, H., Macías, J.L., Espíndola, J.M. et al. The Santa Fe Intrusion and Other Magmatic Bodies Under the Chichón Volcano Area (Mexico): Inferences from Aeromagnetic and New Petrologic-Geochronologic Data. Surv Geophys 41, 859–895 (2020). https://doi.org/10.1007/s10712-020-09591-8

Download citation

  • Received:

  • Accepted:

  • Published:

  • Issue Date:

  • DOI: https://doi.org/10.1007/s10712-020-09591-8

Keywords

Search

Navigation