FN Archimer Export Format
PT J
TI Crustal structure of a super-slow spreading centre: a seismic refraction study of Mohns Ridge, 72 degrees N
BT 
AF KLINGELHOFER, Frauke
   GELI, Louis
   MATIAS, Luis
   STEINSLAND, N
   MOHR, J
AS 1:;2:;3:;4:;5:;
FF 1:;2:PDG-DRO-GM-GEOPHYSIQUE;3:PDG-DRO-GM-GEOPHYSIQUE;4:;5:;
C1 IFREMER, Dept Geosci Marines, Plouzane, France.
   Univ Lisbon, CGUL, P-1699 Lisbon, Portugal.
   Univ Bergen, Inst Solid Earth Phys, N-5020 Bergen, Norway.
C2 IFREMER, FRANCE
   UNIV LISBON, PORTUGAL
   UNIV BERGEN, NORWAY
SI BREST
SE PDG-DRO-GM-GEOPHYSIQUE
IN WOS Ifremer jusqu'en 2018
   copubli-europe
IF 1.544
TC 70
UR https://archimer.ifremer.fr/doc/2000/publication-681.pdf
LA English
DT Article
DE ;Seismic refraction;Oceanic crust;Mohns Ridge;Mantle
AB A series of eight high-resolution seismic refraction profiles from the ultra-slow spreading (16 mm yr(-1) full spreading rate) Mohns Ridge in the Norwegian-Greenland Sea has been treated with modern inversion methods. The profiles were shot parallel to the ridge at an off-axis distance of 0-135 km corresponding to crustal ages of 0-22 Ma. The resulting models are constrained by synthetic seismograms and gravity modelling.The crustal thickness in all profiles is well below the global average for typical oceanic crust, and shows a high variability with a mean thickness of 4.0 +/- 0.5 km. This is mainly due to a very thin and variable lower crustal layer (Layer 3). Generally, the crust is thicker beneath basement highs and thinner beneath basins, implying local isostatic compensation. The top of the basement (Layer 2a) consists of a zone with low P-wave velocities (2.5-3.0 km s(-1)). The mean thickness of this layer decreases with distance from the ridge. Beneath it lies a layer with slightly higher velocities (Layer 2b). Its thickness shows less variability along a given profile and an overall increase with age. The combined average thickness of the upper two layers remains nearly constant, indicating that the boundary between Layer 2a and 2b may represent an alteration front.Upper mantle velocities are generally slow, around 7.5 km s(-1). For the profile directly within the rift valley, a model without a third layer, incorporating a constant gradient up to upper mantle velocities, and a model with a Moho depth inferred from neighbouring profiles and upper mantle velocity as slow as 7.2 km s(-1) fit the seismic and gravity data equally well. The crustal structure is not mature below the ridge. These observations support previous models suggesting the presence of low densities and velocities at about 2 km below the rift axis. Poisson's ratios determined from converted S-wave modelling are incompatible with a Layer 3 consisting of purely serpentinized peridotite. However, a volume fraction of 10-40 per cent serpentinite cannot be ruled out.
PY 2000
PD MAY
SO Geophysical Journal International
SN 0956-540X
PU Blackwell science
VL 141
IS 2
UT 000086981500019
BP 509
EP 526
DI 10.1046/j.1365-246x.2000.00098.x
ID 681
ER

EF