Open AccessStrontium isotope constraints on fluid flow in the sheeted dike complex of fast spreading crust: Pervasive fluid flow at Pito Deep
Author(s) -
Barker A. K.,
Coogan L. A.,
Gillis K. M.,
Weis D.
Publication year - 2008
Publication title -
geochemistry, geophysics, geosystems
Language(s) - English
Resource type - Journals
SCImago Journal Rank - 1.928
H-Index - 136
ISSN - 1525-2027
DOI - 10.1029/2007gc001901
Subject(s) - geology , crust , dike , hydrothermal circulation , oceanic crust , tectonics , fluid dynamics , isotopes of strontium , petrology , geochemistry , seawater , protolith , isotope , subduction , seismology , physics , mechanics , oceanography , quantum mechanics
Fluid flow through the axial hydrothermal system at fast spreading ridges is investigated using the Sr‐isotopic composition of upper crustal samples recovered from a tectonic window at Pito Deep (NE Easter microplate). Samples from the sheeted dike complex collected away from macroscopic evidence of channelized fluid flow, such as faults and centimeter‐scale hydrothermal veins, show a range of 87 Sr/ 86 Sr from 0.7025 to 0.7030 averaging 0.70276 relative to a protolith with 87 Sr/ 86 Sr of ∼0.7024. There is no systematic variation in 87 Sr/ 86 Sr with depth in the sheeted dike complex. Comparison of these new data with the two other localities that similar data sets exist for (ODP Hole 504B and the Hess Deep tectonic window) reveals that the extent of Sr‐isotope exchange is similar in all of these locations. Models that assume that fluid‐rock reaction occurs during one‐dimensional (recharge) flow lead to significant decreases in the predicted extent of isotopic modification of the rock with depth in the crust. These model results show systematic misfits when compared with the data that can only be avoided if the fluid flow is assumed to be focused in isolated channels with very slow fluid‐rock exchange. In this scenario the fluid at the base of the crust is little modified in 87 Sr/ 86 Sr from seawater and thus unlike vent fluids. Additionally, this model predicts that some rocks should show no change from the fresh‐rock 87 Sr/ 86 Sr, but this is not observed. Alternatively, models in which fluid‐rock reaction occurs during upflow (discharge) as well as downflow, or in which fluids are recirculated within the hydrothermal system, can reproduce the observed lack of variation in 87 Sr/ 86 Sr with depth in the crust. Minimum time‐integrated fluid fluxes, calculated from mass balance, are between 1.5 and 2.6 × 10 6 kg m −2 for all areas studied to date. However, new evidence from both the rocks and a compilation of vent fluid compositions demonstrates that some Sr is leached from the crust. Because this leaching lowers the fluid 87 Sr/ 86 Sr without changing the rock 87 Sr/ 86 Sr, these mass balance models must underestimate the time‐integrated fluid flux. Additionally, these values do not account for fluid flow that is channelized within the crust.