Galápagos spreading centre
In plate tectonics, the Galápagos spreading centre, Galápagos spreading center or Cocos–Nazca rift is a divergent boundary that forms the western part of the Cocos–Nazca spreading centre between the Cocos and Nazca plates. It extends for over 1800 km (1100 miles) from close to the eastern boundary of the Pacific plate, the East Pacific Rise, in the west, to the Inca Transform in the east. It consists of two main ridge segments linked by the Galápagos Transform.[1][2]
Geometry
[edit]The Galápagos spreading centre (GSC) consists of two main sections, linked by the Galápagos Transform (GT). The western section extends from the propagating tip of the GSC (about 30 km east of the East Pacific Rise) for about 1200 km (750 miles) to the northern end of the transform. On the basis of changes in character along its length, this section has been divided into three "provinces". The western province, which runs with a trend of N092°E[clarification needed] from the western tip to about 95.5° W, is characterised by multiple short segments with mainly left-stepping offsets[clarification needed] between them, but with overlaps and no transforms. In this part of the GSC there is a well-developed axial valley. The middle province from 95.5° W to about 93.2° W shows a transition towards a central ridge development, a small rotation of the axis to N096°E and many small left-stepping offsets.[clarification needed] The eastern province runs from 93.2° W to 91.0° W, showing small right-stepping offsets, a further rotation to N100°E and a fully developed central ridge. The western end of the GSC forms part of the boundary to the clockwise-rotating Galápagos microplate.[3]
The eastern section runs for about 600 km from the southern end of the GT to the Inca Transform with a constant trend of N097°E. There are two main segments that overlap with a left-stepping offset with no transform developed at 87° W. To the west of this overlap, the GSC is divided into a further six segments. The easternmost three segments are characterised by multiple alternating low-relief valleys and ridges. The westernmost segments all have an axial valley within a single ridge.[3]
The ~95 km long Galápagos Transform links the two main sections of the GSC. It is somewhat oblique to the direction of spreading in the two segments that it links, suggesting that it is unlikely to be a true transform. It is thought to have formed as a result of one or more southward jumps of the eastern GSC towards the Galápagos hotspot.[3]
Galápagos microplate
[edit]
The 13,000 km2 Galápagos microplate lies at the western end of the GSC. It is bounded to the west by strands of the East Pacific Rise, to the southeast by the Dietz Volcanic Ridge and the Dietz Deep rift, and to the north by the GSC.[4] Another separate, smaller microplate has also been proposed , bounded to the north by an incipient rift structure. The main (southern) microplate rotates clockwise, while the northern microplate rotates anticlockwise.[5]
The westward propagation of the GSC has apparently stalled, getting no closer to the East Pacific Rise during the last few million years, due to interactions with the microplate.[6]
Galápagos hotspot
[edit]
The Galápagos hotspot has been sited close to the GSC since the break-up of the Farallon plate as demonstrated by the Cocos and Carnegie aseismic ridges.[7] More recently the hotspot has been located to the south of the GSC resulting in an overall relative northward movement of the GCS. However, the eastern section of the GSC shows evidence of repeated ridge jumps, with the active spreading location moving episodically to the south, towards the hotspot, creating the Galápagos transform.
Between the Galápagos islands and the GSC, a large group of volcanic seamounts are developed, known as the Northern Galápagos Volcanic Province (NGVP). The seamounts are sited along a series of ridges that fan out from just north of the islands, terminating at the GSC. The most prominent and westerly of these is the Wolf–Darwin lineament, on which both Wolf Island and Darwin Island are located.[8] The ridges are interpreted to represent the surface expression of channels along which magma is moving from the hotspot to the GSC.[9]
References
[edit]- ^ Peirce, C.; Tedd, J.C.; Hobbs, R.W. (2023). "Structure and dynamics of the Ecuador Fracture Zone, Panama Basin". Geophysical Journal International. 235 (2): 1519–1540. doi:10.1093/gji/ggad315.
- ^ Baker, E.T.; Hayman, R.M.; Resing, J.A.; White, S.M.; Walker, S.L.; Macdonald, K.C.; Nakamura, K. (2008). "High-resolution surveys along the hot spot–affected Galápagos Spreading Center: 1. Distribution of hydrothermal activity". Geochemistry, Geophysics and Geosystems. 9 (9). doi:10.1029/2008GC002028.
- ^ a b c Christie, D.M.; Werner, R.; Hauff, F.; Hoernle, K.; Hanan, B.B. (2005). "Morphological and geochemical variations along the eastern Galápagos Spreading Center". Geochemistry, Geophysics and Geosystems. 6 (1): Q01006. doi:10.1029/2004GC000714.
- ^ Lonsdale, P. (1988). "Structural pattern of the Galapagos microplate and evolution of the Galapagos triple junctions". Journal of Geophysical Research: Solid Earth. 93 (B11): 13551–13574. doi:10.1029/JB093iB11p13551.
- ^ Klein, E.M.; Smith, D.M.; Williams, C.M.; Schouten, H. (2005). "Counter-rotating microplates at the Galapagos triple junction". Nature. 433 (7028): 855–858. Bibcode:2005Natur.433..855K. doi:10.1038/nature03262. PMID 15729339. S2CID 4424588.
- ^ Smith, D.K.; Schouten, H.; Parnell-Turner, R.; Klein, E.M.; Cann, J.; Dunham, C.; Alodia, G.; Blasco, I.; Wernette, B.; Zawadzki, D.; Latypova, E.; Afshar, S.; Curry, S. (2020). "The Evolution of Seafloor Spreading Behind the Tip of the Westward Propagating Cocos-Nazca Spreading Center". Geochemistry, Geophysics and Geosystems. 21 (6): e2020GC008957. doi:10.1029/2020GC008957.
- ^ Harpp, K. S.; Wanless, V. D.; Otto, R. H.; Hoernle, K.; Werner, R. (2005). "The Cocos and Carnegie Aseismic Ridges: a Trace Element Record of Long-term Plume-Spreading Center Interaction". Journal of Petrology. 46 (1): 109–133. doi:10.1093/petrology/egh064.
- ^ Mittelstaedt, E.; Soule, S.; Harpp, K.; Fornari, D.; McKee, C.; Tivey, M.; Geist, D.; Kurz, M.D.; Sinton, C.; Mello, C. (2012). "Multiple expressions of plume-ridge interaction in the Galápagos: Volcanic lineaments and ridge jumps". Geochemistry, Geophysics and Geosystems. 13 (5): Q05018. doi:10.1029/2012GC004093.
- ^ Mittal, T.; Richards, M.A. (2017). "Plume-ridge interaction via melt channelization at Galápagos and other near-ridge hotspot provinces". Geochemistry, Geophysics and Geosystems. 18 (4): 1711–1738. doi:10.1002/2016GC006454.