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Natland, James H; Adamson, Andrew C; Laverne, Christine; Melson, William G; O'Hearn, Timothy (1983): Geochemistry and minerals at DSDP Legs 68-70 Holes [dataset publication series]. PANGAEA, https://doi.org/10.1594/PANGAEA.817014, Supplement to: Natland, JH et al. (1983): A compositionally nearly steady-state magma chamber at the Costa Rica Rift: Evidence from basalt glass and mineral data, Deep Sea Drilling Project Sites 501, 504, and 505. In: Cann, JR; Langseth, MG; Honnorez, J; Von Herzen, RP; White, SM; et al. (eds.), Initial Reports of the Deep Sea Drilling Project (U.S. Govt. Printing Office), 69, 811-858, https://doi.org/10.2973/dsdp.proc.69.154.1983

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Abstract:
The compositions of natural glasses and phenocrysts in basalts from Deep Sea Drilling Project Sites 501, 504, and 505, near the Costa Rica Rift, constitute evidence for the existence of a periodically replenished axial magma chamber that repeatedly erupted lavas of remarkably uniform composition. Magma compositions were affected by three general components: (1) injected magmas carrying (in decreasing order of abundance) Plagioclase, olivine, and chrome-spinel phenocrysts (spinel assemblage); (2) injected magmas carrying Plagioclase, clinopyroxene, and olivine phenocrysts, but no spinel (clinopyroxene assemblage); and (3) moderately evolved hybrids in the magma chamber itself. The compositions of the injected phenocrysts and minerals in glomerocrysts are as follows: Plagioclase - An85-94; olivine - Fo87-89; clinopyroxene - high Cr2O3 (0.7-1.1%), endiopside (Wo42En51Fs7), and aluminous chromian spinel (Cr/Cr + Al = 0.3). These minerals resemble those thought to occur in upper mantle sources (9 kbars and less) of ocean-ridge basalts and to crystallize in magmas near those sources. In the magma chamber, more sodic Plagioclase (An79-85), less magnesian olivine (Fo81-86) and low-Cr2O3 (0.1-0.4%) clinopyroxene formed rims on these crystals, grew as other phenocrysts, and formed cumulus segregations on the walls and floors of the magma chamber. In the spinel-assemblage magmas, magnesiochromite (Cr/Cr + Al = 0.4-0.5) also formed. Some cumulus segregations were later entrained in lavas as xenoliths.
The glass compositions define 16 internally homogeneous eruptive units, 13 of which are in stratigraphic order in a single hole, Hole 504B, which was drilled 561.5 meters into the ocean crust. These units are defined as differing from each other by more than analytical uncertainty in one or more oxides. However, many of the glass groups in Hole 504B show virtually no differences in TiO2 contents, Mg/Mg + Fe2+, or normative An/An + Ab, all of which are sensitive indicators of crystallization differentiation. The differences are so small that they are only apparent in the glass compositions; they are almost completely obscured in whole-rock samples by the presence of phenocrysts and the effects of alteration. Moreover, several of the glass units at different depths in Hole 504B are compositionally identical, with all oxides falling within the range of analytical uncertainty, with only small variations in the rest of the suite. The repetition of identical chemical types requires (1) very regular injection of magmas into the magma chamber, (2) extreme similarity of injected magmas, and (3) displacement of very nearly the same proportion of the magmas in the chamber at each injection. Numerical modeling and thermal considerations have led some workers to propose the existence of such conditions at certain types of spreading centers, but the lava and glass compositions at Hole 504B represent the first direct evidence revealed by drilling of the existence of a compositionally nearly steady-state magma chamber, and this chapter examines the processes acting in it in some detail.
The glass groups that are most similar are from clinopyroxene-assemblage lavas, which have a range of Mg/Mg + Fe2"1" of 0.59 to 0.65. Spinel-assemblage basalts are less evolved, with Mg/Mg + Fe2+ of 0.65 to 0.69, but both types have nearly identical normative An/An + Ab (0.65-0.66). However, the two lava types contain megacrysts (olivine, Plagioclase, clinopyroxene) that crystallized from melts with Mg/Mg + Fe2+ values of 0.70 to 0.72. Projection of glass compositions into ternary normative systems suggests that spinel-assemblage magmas originated deeper in the mantle than clinopyroxene-assemblage magmas, and mineral data indicate that the two types followed different fractionation paths before reaching the magma chamber. The two magma types therefore represent neither a low- nor a high-pressure fractionation sequence. Some of the spinel-assemblage magmas may have had picritic parents, but were coprecipitating all of the spinel-assemblage phenocrysts before reaching the magma chamber. Clinopyroxene-assemblage magmas did not have picritic parents, but the compositions of phenocrysts suggest that they originated at about 9 kbars, near the transition between plagioclase peridotite and spinel peridotite in the mantle.
Two glass groups have higher contents of alkalis, TiO2, and P2O5 than the others, evidently as a result of the compositions of mantle sources. Eruption of these lavas implies that conduits and chambers containing magmas from dissimilar sources were not completely interconnected on the Costa Rica Rift.
The data are used to draw comparisons with the East Pacific Rise and to consider the mechanisms that may have prevented the eruption of ferrobasalts at these sites.
Project(s):
Deep Sea Drilling Project (DSDP)
Coverage:
Median Latitude: 1.359444 * Median Longitude: -83.742870 * South-bound Latitude: 1.226800 * West-bound Longitude: -83.790000 * North-bound Latitude: 1.920000 * East-bound Longitude: -83.730000
Date/Time Start: 1979-07-08T00:00:00 * Date/Time End: 1979-12-04T00:00:00
Event(s):
68-501 * Latitude: 1.227200 * Longitude: -83.734300 * Date/Time: 1979-07-08T00:00:00 * Elevation: -3457.0 m * Penetration: 337.1 m * Recovery: 70.5 m * Location: North Pacific/FLANK * Campaign: Leg68 * Basis: Glomar Challenger * Method/Device: Drilling/drill rig (DRILL) * Comment: 19 cores; 137.7 m cored; 0.5 m drilled; 51.2 % recovery
69-504A * Latitude: 1.226800 * Longitude: -83.732500 * Date/Time: 1979-09-24T00:00:00 * Elevation: -3458.0 m * Penetration: 277 m * Recovery: 207 m * Campaign: Leg69 * Basis: Glomar Challenger * Method/Device: Drilling/drill rig (DRILL)
69-504B * Latitude: 1.227200 * Longitude: -83.730200 * Date/Time: 1979-10-07T00:00:00 * Elevation: -3460.0 m * Penetration: 489 m * Recovery: 262 m * Campaign: Leg69 * Basis: Glomar Challenger * Method/Device: Drilling/drill rig (DRILL)
License:
Creative Commons Attribution 3.0 Unported (CC-BY-3.0)
Size:
10 datasets

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Datasets listed in this publication series

  1. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 13A) Geochemistry of DSDP Sample 68-501-15-3,63-65 of glass inclusions in plagioclase megacrysts. https://doi.org/10.1594/PANGAEA.817012
  2. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 13B) Geochemistry of DSDP Sample 68-501-15-3,63-65 glass. https://doi.org/10.1594/PANGAEA.817013
  3. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 12) Geochemistry and minerals of clinopyroxenes at DSDP Hole 69-504B. https://doi.org/10.1594/PANGAEA.817011
  4. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 9) Geochemistry of Cr-spinels at DSDP Holes 70-504B and 68-501. https://doi.org/10.1594/PANGAEA.817008
  5. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 5) Geochemistry of olivines at DSDP Holes 70-504B and 69-505B. https://doi.org/10.1594/PANGAEA.817004
  6. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 1) Geochemistry of basaltic glasses at DSDP Legs 68-70 Holes. https://doi.org/10.1594/PANGAEA.817002
  7. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 10) Geochemistry of olivine at DSDP Legs 68-70. https://doi.org/10.1594/PANGAEA.817009
  8. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 11) Geochemistry of plagioclases at DSDP Legs 68-70. https://doi.org/10.1594/PANGAEA.817010
  9. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 7) Geochemistry of clinopyroxenes at DSDP Legs 69-70 Holes. https://doi.org/10.1594/PANGAEA.817007
  10. Natland, JH; Adamson, AC; Laverne, C et al. (1983): (Table 6) Geochemistry of plagioclases at DSDP Legs 69-70 Holes. https://doi.org/10.1594/PANGAEA.817006