Kimberlite hosts two populations of olivine that are distinguished on the basis of grain size and morphology; the populations are commonly described genetically as xenocrysts and phenocrysts. Recent studies of zoning patterns in kimberlitic olivine phenocrysts have cast doubt on the actual origins of the smaller olivine crystals. Here, we elucidate the nature and origins of the textural and chemical zonation that characterize both populations of olivine. Specifically, we show that both olivine-I and olivine-II feature chemically distinct overgrowths resulting from magmatic crystallization on pre-existing olivine xenocrysts. These results suggest that the total volume of olivine crystallized during transport is substantially lower (≤5%) than commonly assumed (e.g. ~25%), and that crystallization is dominantly heterogeneous. This reduces estimates of the Mg# in primitive kimberlite melt to more closely reconcile with measured phenocryst compositions. Several additional textures are observed in olivine, and include: sealed cracks, healed cracks, phases trapping in cracks, rounded grains, overgrowths and phase trapping in overgrowths. These features record processes that operate in kimberlite during ascent, and from these features we create a summary model for kimberlite ascent: • Olivine is incorporated into kimberlitic melts at great depths as peridotitic mantle xenoliths. • Shortly after the incorporation of these xenocrysts the tensile strength of the crystals within xenoliths is reached at a minimum of 20 km from its source. Disaggregation of mantle xenoliths producing xenocrysts is facilitated by expansion of the minerals within the xenoliths. • The void space produced by the failure of the crystals is filled with melt and crystals consisting of primary carbonate (high-Sr), chromite and spinel crystals. The carbonate later crystallizes to produce sealed fractures. • Subsequent decompression causes cracks that are smaller than the sealed cracks and are preserved as healed cracks that crosscut sealed cracks. • Mechanical rounding of the xenocrysts post-dates, and/or occurs contemporaneously with decompression events that cause cracking. • Saturation of olivine produces rounded overgrowths on large xenocrysts, euhedral overgrowths on smaller xenocrysts, and a volumetrically minor population of olivine phenocrysts. Olivine growth traps fluid, solid and melt inclusions. Calculations based on these relationships suggest that the melt saturates with olivine at a maximum depth of 20 km and a minimum depth of 7 km.

Kimberlite hosts two populations of olivine that are distinguished on the basis of grain size and morphology; the populations are commonly described genetically as xenocrysts and phenocrysts. Recent studies of zoning patterns in kimberlitic olivine phenocrysts have cast doubt on the actual origins of the smaller olivine crystals. Here, we elucidate the nature and origins of the textural and chemical zonation that characterize both populations of olivine. Specifically, we show that both olivine-I and olivine-II feature chemically distinct overgrowths resulting from magmatic crystallization on pre-existing olivine xenocrysts. These results suggest that the total volume of olivine crystallized during transport is substantially lower (≤5%) than commonly assumed (e.g. ~25%), and that crystallization is dominantly heterogeneous. This reduces estimates of the Mg# in primitive kimberlite melt to more closely reconcile with measured phenocryst compositions. Several additional textures are observed in olivine, and include: sealed cracks, healed cracks, phases trapping in cracks, rounded grains, overgrowths and phase trapping in overgrowths. These features record processes that operate in kimberlite during ascent, and from these features we create a summary model for kimberlite ascent: • Olivine is incorporated into kimberlitic melts at great depths as peridotitic mantle xenoliths. • Shortly after the incorporation of these xenocrysts the tensile strength of the crystals within xenoliths is reached at a minimum of 20 km from its source. Disaggregation of mantle xenoliths producing xenocrysts is facilitated by expansion of the minerals within the xenoliths. • The void space produced by the failure of the crystals is filled with melt and crystals consisting of primary carbonate (high-Sr), chromite and spinel crystals. The carbonate later crystallizes to produce sealed fractures. • Subsequent decompression causes cracks that are smaller than the sealed cracks and are preserved as healed cracks that crosscut sealed cracks. • Mechanical rounding of the xenocrysts post-dates, and/or occurs contemporaneously with decompression events that cause cracking. • Saturation of olivine produces rounded overgrowths on large xenocrysts, euhedral overgrowths on smaller xenocrysts, and a volumetrically minor population of olivine phenocrysts. Olivine growth traps fluid, solid and melt inclusions. Calculations based on these relationships suggest that the melt saturates with olivine at a maximum depth of 20 km and a minimum depth of 7 km.

Volatiles are fundamental to many aspects of kimberlite magmatism. However, the volatile compositions and concentrations are poorly defined. Enrichment of H in kimberlitic olivines, many of which are xenocrysts, suggests high water content, but the extent to which H exchanges between these xenocrysts and kimberlite magmas remains unclear. This study investigates zonation of H in kimberlite-hosted xenolith and macrocrystic olivines using Fourier transform infrared spectroscopy to constrain the extent of re-equilibration. Data show that, depending on locality, xenolith olivines exhibit either no H-zonation, or substantial H-depletion in their rims. Macrocrysts feature similar trends to xenolith olivines from the same intrusion. In terms of the rim:core ratio of H, strongly zoned olivines average ~0.5, whereas poorly zoned olivines average at ~0.9 (macrocrysts) or 1.0 (xenolith olivines). Locality-specific H-zonation could result from different magmatic thermal regimes, water concentrations, or ascent durations. If the magmas that contained weakly zoned olivines were anhydrous, their restricted zoning requires ascent durations (< 20 min at 1100 °C) that are considerably shorter than published estimates (~1-24 hr at 1100 °C). These findings suggest that elevated magmatic water concentrations minimized loss of H from olivine in these kimberlites, showing that non-equilibrated xenocrysts could indirectly record high water concentrations in the form of weak H-zonation. Strong H-depletion patterns in olivines from other kimberlites may reflect lower initial magmatic water concentrations, or loss of fluid to country rocks. Future studies could compare H-zonation to temperature and ascent rate estimates, and field relationships to better elucidate the causes of locality-specific H-zonation. An apparent correlation between diamond grade and H-zonation warrants further investigation. / This thesis includes an Electronic Appendix, available at http://dalspace.library.dal.ca

Kimberlite hosts two populations of olivine that are distinguished on the basis of grain size and morphology; the populations are commonly described genetically as xenocrysts and phenocrysts. Recent studies of zoning patterns in kimberlitic olivine phenocrysts have cast doubt on the actual origins of the smaller olivine crystals. Here, we elucidate the nature and origins of the textural and chemical zonation that characterize both populations of olivine. Specifically, we show that both olivine-I and olivine-II feature chemically distinct overgrowths resulting from magmatic crystallization on pre-existing olivine xenocrysts. These results suggest that the total volume of olivine crystallized during transport is substantially lower (≤5%) than commonly assumed (e.g. ~25%), and that crystallization is dominantly heterogeneous. This reduces estimates of the Mg# in primitive kimberlite melt to more closely reconcile with measured phenocryst compositions. Several additional textures are observed in olivine, and include: sealed cracks, healed cracks, phases trapping in cracks, rounded grains, overgrowths and phase trapping in overgrowths. These features record processes that operate in kimberlite during ascent, and from these features we create a summary model for kimberlite ascent: • Olivine is incorporated into kimberlitic melts at great depths as peridotitic mantle xenoliths. • Shortly after the incorporation of these xenocrysts the tensile strength of the crystals within xenoliths is reached at a minimum of 20 km from its source. Disaggregation of mantle xenoliths producing xenocrysts is facilitated by expansion of the minerals within the xenoliths. • The void space produced by the failure of the crystals is filled with melt and crystals consisting of primary carbonate (high-Sr), chromite and spinel crystals. The carbonate later crystallizes to produce sealed fractures. • Subsequent decompression causes cracks that are smaller than the sealed cracks and are preserved as healed cracks that crosscut sealed cracks. • Mechanical rounding of the xenocrysts post-dates, and/or occurs contemporaneously with decompression events that cause cracking. • Saturation of olivine produces rounded overgrowths on large xenocrysts, euhedral overgrowths on smaller xenocrysts, and a volumetrically minor population of olivine phenocrysts. Olivine growth traps fluid, solid and melt inclusions. Calculations based on these relationships suggest that the melt saturates with olivine at a maximum depth of 20 km and a minimum depth of 7 km. / Science, Faculty of / Earth, Ocean and Atmospheric Sciences, Department of / Graduate

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