Thy, Peter (2003): Mineral composition and major element oxides of gabbros from ODP Hole 179-1105A, southwest Indian Ridge. PANGAEA, https://doi.org/10.1594/PANGAEA.787241, Supplement to: Thy, P (2003): Igneous petrology of gabbros from Hole 1105A: oceanic magma chamber processes. In: Casey, JF; Miller, DJ (eds.) Proceedings of the Ocean Drilling Program, Scientific Results, College Station, TX (Ocean Drilling Program), 179, 1-76, https://doi.org/10.2973/odp.proc.sr.179.017.2003
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Hole 1105A penetrated 158 m of gabbros at a site offset 1.3 km east-northeast from Hole 735B on the Atlantis Bank near the Atlantis II Fracture Zone. A total of 118 m of dominantly medium- to coarse-grained intercalated Fe-Ti oxide gabbro and olivine gabbro was recovered from Hole 1105A that shows many petrographic features similar to those recovered from the upper part of Hole 735B. The main rock types are distinguished based on the constituent cumulus phases, with the most primitive gabbros consisting of olivine, plagioclase, and clinopyroxene. The inferred crystallization order is subsequently Fe-Ti oxides (ilmenite and titanomagnetite), followed by orthopyroxene, then apatite, and finally biotite. Orthopyroxene appears to replace olivine in a narrow middle interval. The magmatic evolution is likewise reflected in the mineral compositions. Plagioclase varies from An66 to An28. Olivine varies from Fo78 to Fo35. The gap in olivine crystallization occurs between Fo46 and Fo40 and coincides approximately with the appearance of orthopyroxene (~En50). The clinopyroxenes show large compositional variation in Mg/(Mg + Fe total) from 0.84 to 0.51. The nonquadrilateral cations of clinopyroxene similarly show large variations with Ti increasing for the olivine gabbros and decreasing for the Fe-Ti oxide gabbros with the decrease in Mg/(Mg + Fe total). The apatites are mainly flourapatites. The compositional variation in the gabbros is interpreted as a comagmatic suite resulting from fractional crystallization. Pyroxene geothermometry suggests equilibration temperatures from 1100°C and below. The coexisting Fe-Ti oxide minerals indicate subsolidus equilibration temperatures from 900°C for olivine gabbros to 700°C for the most evolved apatite-bearing gabbros. The cryptic variation in the olivine gabbros defines two or three lenses, 40 to 60 m thick, each characterized by a distinct convex zoning with a lower segment indicating upward reverse fractionation, a central maximum, and an upper segment showing normal fractionation. The Fe-Ti oxide gabbros show cryptic variations independent of the host olivine gabbros and reveal a systematic upward normal fractionation trend transgressing host olivine gabbro boundaries. Forward fractional crystallization modeling, using a likely parental magma composition from the Atlantis II Fracture Zone (MgO = 7.2 wt%; Mg/[Mg + Fe2+] = 0.62), closely matches the compositions of coexisting olivine, plagioclase, and clinopyroxene. This modeling suggests cosaturation of olivine, plagioclase, and clinopyroxene from 1155°C and the addition of Fe-Ti oxides from 1100°C. The liquid line of descent initially shows increasing FeO with moderately increasing SiO2. After saturation of Fe-Ti oxides, the liquid strongly decreases in FeO and TiO2 and increases in SiO2, reaching dacitic compositions at ~10% liquid remaining. The calculations indicate that formation of olivine gabbros can be accounted for by <65% fractionation and that only the residual 35% liquid was saturated in Fe-Ti oxides. The modeling of the solid fractionation products shows that both the olivine gabbro and the Fe-Ti oxide gabbros contain very small amounts of trapped liquid (<5%). The implications are that the gabbros represent crystal mush that originated in a recharging and tapping subaxial chamber. Compaction and upward melt migration in the crystal mush appear to have been terminated with relatively large amounts of interstitial liquid remaining in the upper parts of the cumulate mush. This termination may have been caused by tectonic disturbances, uplift, and associated withdrawal of magma into the subaxial dike and sill system. Prolonged compaction and cooling of the trapped melt in the mush formed small differentiated bodies and lenses by pressure release migration and crystallization along syntectonic channels. This resulted in differentiation products along lateral and vertical channelways in the host gabbro that vary from olivine gabbro, to Fe-Ti oxide gabbro, gabbronorite, and apatite gabbros and show large compositional variations independent of the host olivine gabbros.
Latitude: -32.718910 * Longitude: 57.277530
Date/Time Start: 1998-05-02T06:50:00 * Date/Time End: 1998-05-10T15:50:00
179-1105A * Latitude: -32.718910 * Longitude: 57.277530 * Date/Time Start: 1998-05-02T06:50:00 * Date/Time End: 1998-05-10T15:50:00 * Elevation: 0.0 m * Penetration: 158 m * Recovery: 118.43 m * Location: Indian Ocean * Campaign: Leg179 * Basis: Joides Resolution * Device: Drilling/drill rig (DRILL) * Comment: 30 cores; 143 m cored; 15 m drilled; 82.8 % recovery
Datasets listed in this publication series
- Thy, P (2003): (Table T1) Silicate mineral compositions of ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787234
- Thy, P (2003): (Table T2) Major element oxides of cumulus plagioclases from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787235
- Thy, P (2003): (Table T3) Major element oxides of cumulus pyroxene from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787236
- Thy, P (2003): (Table T4) Major element oxides of cumulus olivine from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787237
- Thy, P (2003): (Table T5) Major element oxides of coexisting ilmenite and titanomagnetite from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787238
- Thy, P (2003): (Table T6) Major element oxides of cumulus apatite from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787239
- Thy, P (2003): (Table T7) Major element oxides and number of ions of cumulus biotite from ODP Hole 179-1105A. https://doi.org/10.1594/PANGAEA.787240