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Geology and Tectonics of Northwestern South America pp 749–832Cite as

Morphotectonic and Orogenic Development of the Northern Andes of Colombia: A Low-Temperature Thermochronology Perspective

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Part of the book series: Frontiers in Earth Sciences ((FRONTIERS))

Abstract

Landscapes in mountain belts evolve through complex feedback mechanisms between internal and external processes. Modern orogenic belts, such as the Andes, are the result of millions of years of continuing internal and external processes. Therefore, mountain ranges are rich repositories of geomorphic and tectonic information. Established techniques in low temperature thermochronology (LTTC), e.g., fission-track and (U-Th)/He dating, present novel opportunities to quantitatively explore key morphotectonic processes in the upper crust, e.g., the cooling of rocks as they move toward the Earth’s surface during exhumation, via erosion, normal faulting, and/or crustal thinning. We address the Late Mesozoic-Cenozoic morphotectonic and orogenic history of the Northern Andes of Colombia using detailed compilations and analysis of existing LTTC datasets, in an effort to define the spatial distribution, timing, and magnitude of the main orogenic phases in the region, while providing an up-to-date morphotectonic picture of the Northern Andes.

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Notes

  1. 1.

    We use the term uplift (and other associated terminology) in the sense defined by England and Molnar (1990) as follows: Surface uplift is the displacement of the average elevation of the landscape with respect to mean sea level. Rock uplift is the net displacement of a rock parcel with respect to sea level. Rock uplift is equal to surface uplift under no-erosion and no-deposition conditions, i.e., where no exhumation/burial takes place. Exhumation implies the approximation of the rock parcel to the topographic surface. In that sense, exhumation (also referred to as denudation) can be defined as the difference between rock uplift and surface uplift. A topographic steady-state condition is then achieved when rock uplift and erosion proceed at the same rate to inhibit surface uplift.

  2. 2.

    In this contribution, the term relief is equivalent to topographic relief and refers to the difference between the highest and lowest point in a particular area. In that sense the Andean Region of Colombia is characterized by relief in excess of 5000 m, as the highest points in the Central Cordillera reach elevations close to 5.5 km, whereas the bottoms of valleys such as the Middle Cauca and Middle Magdalena are at ~500 m. Conversely, the Caribbean, (except for the Sierra Nevada de Santa Marta with peaks reaching elevations of more than 5.5 km) Amazonian, and Orinoquia regions possess low topographic relief, i.e., <200 m on average. Local and relative relief are more specific terms, indicating the difference in elevation measured over a specified area. Figure 11.7 illustrates differences in relative relief over the Northern Andes. (For more detail on these definitions, see Summerfield, 2001, and Montgomery 2003).

  3. 3.

    For details on the Romeral Shear Zone, see Chap. 5, Contribution No. 12, in this volume.

  4. 4.

    PLOCO, from its definition in Spanish as “Provincia Litosférica Oceánica Cretácica Occidental” (Gomez et al. 2015b).

  5. 5.

    PLCMG, from its definition in Spanish as “Provincia Litosférica Continental Mesoproterozoica Grenvilliana” (Gomez et al. 2015b).

  6. 6.

    For a detailed account of magmatism in the Northern Andes, see Chap. 4, contribution No. 5, this volume.

  7. 7.

    Worldwide, the SNSM (5750 m) ranks second in elevation, behind the much broader and longer Saint Elias Range (5959 m) in the USA (Alaska) and Canada.

  8. 8.

    For details on erosion/fluvial process in the Magdalena River, see Chap. 8, Contribution No. 17, this volume.

  9. 9.

    Although the nomenclature of orogenetic phases by van der Hammen refers to orogenetic events of continental scale (in the case of the Laramic) and to the gradual consolidation of the Andean topography, we opt to maintain the same terminology in order to avoid confusion. The chronology of some of these phases in van der Hammen (1961) correspond to the Eocene (Incaic) and Miocene (Quechua) in Peru (Mégard 1984).

  10. 10.

    To avoid confusion arising from the use of the terms uplift, exhumation, denudation, etc., please refer to the LTTC section of this contribution. We emphasize that LTTC techniques can be used through several approaches (vertical profiles, sample multiple dating, etc.) to constrain timing and rate(s) of cooling associated with erosional exhumation. When the term “uplift” is used to discuss LTTC datasets in various litho-structural domains of the Colombian Andes, we assume that “surface uplift” (i.e., topographic buildup) is the main trigger of erosional exhumation. In that regard, LTTC data is taken to yield only bulk erosion rates, such as the movement of a rock parcel toward the eroding topographic surface (i.e., exhumation). Therefore, LTTC does not constrain surface uplift with respect to a fixed frame of reference such as sea level. For a detailed discussion on these issues, see England and Molnar (1990), Brown and Summerfield (1997), and Reniers and Brandon (2006).

  11. 11.

    Instituto de Investigaciones en Estratigrafía (IIES) at Universidad de Caldas (Colombia), Grupo de Estudios Tectónicos (GET) at Universidad Nacional de Colombia (Medellín, Colombia), University of Florida at Gainesville (Florida, USA), University Grenoble Alpes (Grenoble, France), Agencia Nacional de Hidrocarburos-ANH (Colombia), Universidad EAFIT (Medellín, Colombia)

  12. 12.

    For a detailed location and genesis of plutonic masses in the Northern Andes, see Andean Magmatism, in this volume, Chap. 4, contribution No. 4, and/or Gomez et al. (2015a, b).

  13. 13.

    GET research group at Universidad Nacional de Colombia, unpublished datasets.

  14. 14.

    More detailed descriptions of the litho-structural characteristics of the Santander and Garzón Massifs are available in Chap. 2, Contribution No. 3 in this volume. Additional information on thermotectonic events for the Santander Massif, at deeper crustal levels and in relation to other litho-structural elements of the Maracaibo Block and the Venezuelan Andes, are addressed in Chap. 6 contribution No. 14 in this volume.

  15. 15.

    Further details on the Garzón Massif are found in Chap. 2, Contribution No. 2 of this volume.

  16. 16.

    For details on isolated massifs exhibiting Proterozoic and Paleozoic lithologies, see Chap. 2, Contribution No. 3 of this volume.

Abbreviations

AER:

Age-elevation relationship for LTTC data

AFT:

Apatite fission-track dating

A-PAZ:

Apatite partial annealing zone for fission tracks in FT dating LTTC

AHe:

Apatite uranium-thorium/helium dating

AP:

Antioqueño Plateau

CC:

Central Cordillera

CRFS:

Cauca-Romeral Fault System

EC:

Eastern Cordillera

FT:

Fission-track dating

GOF:

Goodness of fit in LTTC modeling

LA-ICP-MS:

Laser ablation inductively coupled plasma mass spectrometry

LTTC:

Low-temperature thermochronology

Ma:

Mega-annum

MTL:

Mean track length in fission-track analyses

NAB:

Northern Andes Block or NorAndean Block

PAZ:

Partial annealing zone for fission tracks in FT dating LTTC

PCB:

Panama-Chocó Block

PLOCO:

From its definition in Spanish as “Provincia Litosférica Oceánica Cretácica Occidental”

PLCMG:

From its definition in Spanish as “Provincia Litosférica Continental Mesoproterozoica Grenvilliana”

PRZ:

Partial retention zone for helium in (U-Th)/He dating LTTC

SNSM:

Sierra Nevada de Santa Marta

SNC:

Sierra Nevada del Cocuy

WC:

Western Cordillera

ZHe:

Zircon uranium-thorium/helium dating

ZFT:

Zircon fission-track dating

Zr-PAZ:

Zircon partial annealing zone for fission tracks in FT dating LTTC

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Authors and Affiliations

  1. Facultad de Minas, Departamento de Geociencias y Medio Ambiente, Universidad Nacional de Colombia, Medellín, Colombia

    Sergio A. Restrepo-Moreno

  2. Department of Geological Sciences, University of Florida, Gainesville, FL, USA

    Sergio A. Restrepo-Moreno

  3. Department of Geological Sciences, University of Florida, Gainesville, FL, USA

    David A. Foster & Kyoungwon Min

  4. ISTerre, Université Grenoble Alps, Grenoble, France

    Matthias Bernet

  5. Facultad de Minas, Departamento de Geociencias y Medio Ambiente, Universidad Nacional de Colombia, Medellín, Colombia

    Santiago Noriega

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  1. Sergio A. Restrepo-Moreno
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  2. David A. Foster
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  3. Matthias Bernet
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  4. Kyoungwon Min
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  5. Santiago Noriega
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Correspondence to Sergio A. Restrepo-Moreno .

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Editors and Affiliations

  1. Consulting Geologist, Department of Geology, University EAFIT, Medellín, Colombia

    Fabio Cediel

  2. Consulting Geologist, Kelowna, BC, Canada

    Robert Peter Shaw

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Restrepo-Moreno, S.A., Foster, D.A., Bernet, M., Min, K., Noriega, S. (2019). Morphotectonic and Orogenic Development of the Northern Andes of Colombia: A Low-Temperature Thermochronology Perspective. In: Cediel, F., Shaw, R.P. (eds) Geology and Tectonics of Northwestern South America. Frontiers in Earth Sciences. Springer, Cham. https://doi.org/10.1007/978-3-319-76132-9_11

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