Site is Loading, Please wait...

Tag: Tectonics

Continental rift evolution (animation)

Continental rift evolution—from inception to breakup—accounting for surface processes and tectonic deformation.

Continental rift evolution—from inception to breakup—accounting for surface processes and tectonic deformation. Shown is the rifting evolution of a regional 3-D model covering upper crust, lower crust, and mantle lithosphere atop an asthenospheric layer. The rift fault network evolves through five major phases: (a) distributed deformation and coalescence, (b) fault system growth, (c) fault system decline and basinward localization, (d) rift migration, and (e) breakup. Sediments not only interact with tectonic deformation but they also record subsidence, block rotation, and rift migration. The visualisation is based on coupled numerical models of geodynamics (ASPECT) and landscape evolution (FastScape). The animation is based on the reference model of Neuharth et al., 2022.

  • Creator: Sascha Brune and Derek Neuharth
  • Original version: 26.05.2024
  • This version: 27.11.2024
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: These animation Sascha Brune and Derek Neuharth is based on Neuharth et al. (2022) and available via the open-access s-ink.org repository.
  • Related reference: Neuharth, D., Brune, S., Wrona, T., Glerum, A., Braun, J., & Yuan, X. (2022). Evolution of Rift Systems and Their Fault Networks in Response to Surface Processes. Tectonics, 41(3), e2021TC007166. https://doi.org/10.1029/2021TC007166

  • Annotation-free version
  • Variable file formats (GIF & MP4)
  • Colour-vision deficiency friendly
  • Readable in black&white
Go to download

Faulty or missing link? – Please report them via a reply below!

Tectonic and mantle convection regimes

Conceptual illustration of different styles (regimes) of tectonics and mantle convection, which are relevant for rocky planets.

Conceptual illustration of different styles (regimes) of tectonics and mantle convection, which are relevant for rocky planets. A planet in “stagnant-lid” regime is covered by a single plate, without any plate boundaries and little to no surface motion. Today, this is likely the case for Mars. A planet evolving in a “heat-pipe” regime, such as Jupiter’s moon Io, is characterised by vertical channels through the lithosphere through which magma erupts to the surface in the form of volcanism. In a “mobile lid” style planet, the multiple cold surface plates are continuously in motion, often with differing (usually higher) velocities than the mantle below. Earth’s ocean-plate tectonics is a subcategory of such a mobile-lid regime, marked by narrow plate boundaries at which plates are either created or recycled back into the mantle. The “squishy-lid” regime is characterised by a strong surface plate that is regionally weakened and deformed by intrusive magmatism. Venus is commonly considered to be in a squishy-lid mantle regime.

  • Vector format versions
  • Dark-background version
  • Transparent-background version
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Subduction zone initiation reconstructions

Subduction zone initiation (SZI) reconstructions for selected events since around 100 Ma. The reconstructed events are based on the whole Earth Sciences community point-of-view of the SZI database.

Subduction zone initiation (SZI) reconstructions for selected events since around 100 Ma. The reconstructed events are based on the whole Earth Sciences community point-of-view of the SZI database (www.SZIdatabase.org). Represented are SZI events of the Pacific subduction realm (Ryukyu at around 6 Ma, Philippine at around 9 Ma, New Hebrides-New Britain at around 10 Ma, Halmahera at around 16 Ma, Tonga-Kermadec at around 48 Ma, and Izu-Bonin-Mariana at around 52 Ma) and remaining SZI events (South-Sandwich at around 40 Ma, Cascadia at around 48 Ma, Lesser Antilles at around 49 Ma, Sunda-Java at around 50 Ma, Aleutian at around 53 Ma, and the two SZI events, Anatolia and Oman, at around 104 Ma). Shown are the new subduction zones (pink lines), other active (solid purple lines) and inactive (dashed purple lines) subduction zones, spreading ridges (solid red lines) and transform faults (red dashed lines).

  • Creator: Valentina Magni
  • This version: 15.11.2022
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Valentina Magni from Crameri et al. (2020) is available via the open-access s-Ink repository.
  • Related reference: Crameri, F., V. Magni, M. Domeier, G.E. Shephard, K. Chotalia, G. Cooper, C. Eakin, A.G. Grima, D. Gürer, A. Király, E. Mulyukova, K. Peters, B. Robert, and M. Thielmann (2020), A transdisciplinary and community-driven database to unravel subduction zone initiation, Nature Communications, 11, 3750. doi:10.1038/s41467-020-17522-9
  • Light & dark versions
  • Individual panel versions
  • Vector format
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Puysegur trench formation

A schematic highlighting the formation of the Puysegur trench, New Zealand, where subduction zone initiation may be both horizontally and then vertically driven, according to a 4D evolution model of this margin.

A schematic highlighting the formation of the Puysegur trench, New Zealand, where subduction zone initiation may be both horizontally and then vertically driven, according to a 4D evolution model of this margin. Its gradual evolution from north to south represents a pseudo-temporal sequence of a forming subduction zone, which naturally spans a few millions of years. In the northern segment, where subduction nucleated, horizontal forces may have dominated, representative of the early stages of subduction initiation. With time, vertical forces took over, propagating along the evolving megathrust and helping to finally form a self-sustaining subduction zone.

  • Vector format
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Subduction zone initiation types

Illustration of the three types of subduction zone initiation (SZI) events, namely Newly destructive, Episodic subduction, and Polarity reversal.

Illustration of the three types of subduction zone initiation (SZI) events. As outlined in Crameri et al. (2020), the SZI type is either Newly destructive (a subduction fault establishing from an intact-plate portion or some sort of non-subduction-related plate weakness), Episodic subduction (a subduction fault establishing at the same location following a previous, yet terminated subduction zone with the same polarity), or Polarity reversal (formation of a new subduction fault with opposite polarity to the fault of the pre-existing, terminating subduction zone).

  • Creator: Fabio Crameri
  • This version: 24.10.2021
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Fabio Crameri from Crameri et al. (2020) is available via the open-access s-Ink repository.
  • Related reference: Crameri, F., V. Magni, M. Domeier, G.E. Shephard, K. Chotalia, G. Cooper, C. Eakin, A.G. Grima, D. Gürer, A. Király, E. Mulyukova, K. Peters, B. Robert, and M. Thielmann (2020), A transdisciplinary and community-driven database to unravel subduction zone initiation, Nature Communications, 11, 3750. doi:10.1038/s41467-020-17522-9
  • Light & dark versions
  • Vector format
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Subduction initiation forcing

The illustration depicts two endmember states in subduction zone initiation: vertically-forced and horizontally-forced subduction initiation.

Illustration of the two endmember states forcing a new subduction zone. The two endmember forcing states characterising subduction zone initiation (SZI) can be described as either vertically-forced or horizontally-forced. As outlined in Crameri et al. (2020), the dominant forcing is either—but never exclusively—vertical (i.e., some combination of plate buoyancy force, the force from any surface load, and vertical mantle-flow force), or horizontal (i.e., some combination of tectonic force and horizontal mantle-flow force).

  • Creator: Fabio Crameri
  • This version: 24.10.2021
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Fabio Crameri from Crameri et al. (2020) is available via the open-access s-Ink repository.
  • Related reference: Crameri, F., V. Magni, M. Domeier, G.E. Shephard, K. Chotalia, G. Cooper, C. Eakin, A.G. Grima, D. Gürer, A. Király, E. Mulyukova, K. Peters, B. Robert, and M. Thielmann (2020), A transdisciplinary and community-driven database to unravel subduction zone initiation, Nature Communications, 11, 3750. doi:10.1038/s41467-020-17522-9
  • Light & dark versions
  • Vector format
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Tectonic plates (relief)

Global maps of tectonic plates of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011).

Tectonic plates map of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011). The Earth’s lithosphere, the rigid outer shell of the planet including the crust and part of the upper mantle, is fractured into about eight major plates and more minor tectonic plates. The relative movement of the plates typically ranges from zero to 10 cm annually. This relative motion causes different deformation at the plate boundaries, which can be grouped into convergence, divergence, and strike-slip motion. At divergent plate boundaries (i.e., spreading ridges), tectonic plates are created, whereas at convergent boundaries (i.e., subduction zones), tectonic plates are recycled back into the Earth’s mantle. Due to their strong deformation, those tectonic plate boundaries are the most common sites for earthquakes and volcanoes.

The Scientific colour map ‘batlow‘ is used to represent individual plates to all readers on this tectonic plates map.

  • Creator: Fabio Crameri
  • This version: 10.09.2021
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Fabio Crameri from Crameri et al. (2020) is available via the open-access s-ink.org repository.
  • Related references:
    Argus, D. F., R. G. Gordon, and C. DeMets (2011), Geologically current motion of 56 plates relative to the no‐net‐rotation reference frame, Geochem. Geophys. Geosyst., 12, Q11001, doi:10.1029/2011GC003751.
    Bird, P. (2003), An updated digital model of plate boundaries, Geochem. Geophys. Geosyst., 4(3), 1027, doi:10.1029/ 2001GC000252.
    Crameri, F., G.E. Shephard, and E.O. Straume (2022, Pre-print), Effective high-quality science graphics from s-Ink.org, EarthArXiv, https://doi.org/10.31223/X51P78
  • Alternative map projections
  • Transparent background
  • Light & dark background versions
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Tectonic plates

Global maps of tectonic plates of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011).

Maps of the tectonic plates of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011). The Earth’s lithosphere, the rigid outer shell of the planet including the crust and part of the upper mantle, is fractured into about eight major plates and more minor tectonic plates. The relative movement of the plates typically ranges from zero to 10 cm annually. This relative motion causes different deformation at the plate boundaries, which can be grouped into convergence, divergence, and strike-slip motion. At divergent plate boundaries (i.e., spreading ridges), tectonic plates are created, whereas at convergent boundaries (i.e., subduction zones), tectonic plates are recycled back into the Earth’s mantle. Due to their strong deformation, those tectonic plate boundaries are the most common sites for earthquakes and volcanoes.

The Scientific colour map ‘batlow‘ is used to represent individual plates to all readers.

  • Creator: Fabio Crameri
  • This version: 10.09.2021
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Fabio Crameri from Crameri et al. (2022) is available via the open-access s-ink.org repository.
  • Related references:
    Argus, D. F., R. G. Gordon, and C. DeMets (2011), Geologically current motion of 56 plates relative to the no‐net‐rotation reference frame, Geochem. Geophys. Geosyst., 12, Q11001, doi:10.1029/2011GC003751.
    Bird, P. (2003), An updated digital model of plate boundaries, Geochem. Geophys. Geosyst., 4(3), 1027, doi:10.1029/ 2001GC000252.
    Crameri, F., G.E. Shephard, and E.O. Straume (2022, Pre-print), Effective high-quality science graphics from s-Ink.org, EarthArXiv, https://doi.org/10.31223/X51P78
  • Alternative map projections
  • Transparent background
  • Light & dark background versions
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Tectonic plates (simple)

Global maps of tectonic plates of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011).

Maps of the tectonic plates of the Earth, consisting of 56 individual plates named according to abbreviations given in Argus et al. (2011). The Earth’s lithosphere, the rigid outer shell of the planet including the crust and part of the upper mantle, is fractured into about eight major plates and more minor tectonic plates. The relative movement of the plates typically ranges from zero to 10 cm annually. This relative motion causes different deformation at the plate boundaries, which can be grouped into convergence, divergence, and strike-slip motion. At divergent plate boundaries (i.e., spreading ridges), tectonic plates are created, whereas at convergent boundaries (i.e., subduction zones), tectonic plates are recycled back into the Earth’s mantle. Due to their strong deformation, those tectonic plate boundaries are the most common sites for earthquakes and volcanoes.
The Scientific colour map ‘batlow‘ is used to represent individual plates to all readers.

  • Creator: Fabio Crameri
  • This version: 10.09.2021
  • License: Attribution-ShareAlike 4.0 International (CC BY-SA 4.0)
  • Specific citation: This graphic by Fabio Crameri from Crameri et al. (2022) is available via the open-access s-ink.org repository.
  • Related references:
    Argus, D. F., R. G. Gordon, and C. DeMets (2011), Geologically current motion of 56 plates relative to the no‐net‐rotation reference frame, Geochem. Geophys. Geosyst., 12, Q11001, doi:10.1029/2011GC003751.
    Bird, P. (2003), An updated digital model of plate boundaries, Geochem. Geophys. Geosyst., 4(3), 1027, doi:10.1029/ 2001GC000252.
    Crameri, F., G.E. Shephard, and E.O. Straume (2022, Pre-print), Effective high-quality science graphics from s-Ink.org, EarthArXiv, https://doi.org/10.31223/X51P78
  • Alternative map projections
  • Transparent background
  • Light & dark background versions
  • Colour-vision deficiency friendly
  • Readable in black&white
Download

Faulty or missing link? – Please report them via a reply below!

Exit mobile version
%%footer%%