Abstract Although glass corrosion resistance has been tested with laboratory methods for decades, investigators are now just beginning to understand the reaction phenomena at or close to saturation with respect to the rate-limiting phase(s). Near saturation, the phenomena that govern element release rates include alkali-hydrogen (species) exchange, differential reactivity of phase-separated glass, and accelerated corrosion rates due to precipitation of key secondary phases. These phenomena were not anticipated by early models of glass dissolution and are incompletely quantified in current rate representations. This review discusses the two over-arching models for glass reactivity, diffusion and surface reaction control, and demonstrates the importance of glass reactivity in terms of glass composition and micro-heterogeneity of the glass. Our conclusion is that surface reaction control best describes the release of elements to solution, but that models based on current interpretations of transition state theory (TST) must be modified to account for reported anomalies in behaviour near saturation.

Abstract The Colli Albani volcano has been active since c . 600 ka and is presently quiescent. Rock stratigraphy indicates that the activity of the volcano has undergone major changes in terms of eruption style, average eruption rate and location of active vents. The chemistry of the Colli Albani products is remarkably mafic, K-rich and silica undersaturated. Nevertheless, the volcano has experienced all types of eruption styles, from plinian explosive paroxysms, to milder strombolian and hawaiian eruptions, to effusive, including large- and small-scale phreatomagmatism. The first period of activity of the volcano is termed the ‘Vulcano Laziale’ period, and lasted from c . 600 ka to c . 355 ka. During this period, the volcanism was predominantly explosive, with an average eruption rate of 1 km 3 ka −1 . At least seven intermediate- to large-volume ignimbrites (VEI 5–7) were erupted and emplaced over an area larger than 1600 km 2 , forming an extensive ignimbrite shield around the central, continuously forming c . 8 × 8 km 2 caldera. The caldera complex and the ignimbrite shield are named the ‘Vulcano Laziale edifice’. The Vulcano Laziale edifice can in turn be subdivided into a lower ‘Pisolitic Tuffs succession’ ( c . 600–500 ka), in which ignimbrites are dominated by large-scale phreatomagmatism associated with the likely presence of an early caldera lake, and an overlying ‘Pozzolane Tuffs succession’, in which ignimbrites show a dominantly magmatic fragmentation style, probably in response to progressive exhaustion of the caldera lake. The typical succession of these mafic ignimbrites is composed of a sub-plinain to plinian basal scoria fall deposit covered by the main dark scoria and ash tabular ignimbrite sheet found as far as >30 km from the caldera rim and across ridges several hundreds metres in elevation, and is characterized by co-ignimbrite breccias at proximal locations. Major ignimbrites erupted with an average interval of c . 40 ka. After each paroxysmal ignimbrite eruption, volcanic activity was predominantly effusive to mild explosive, and was concentrated along peri-caldera fissure systems, forming continuous scoria cone and lava ridges, together with more explosive eruptions from intracaldera vents. The last major caldera-forming eruption of the Vulcano Laziale period occurred at c . 355 ka, emplacing the ignimbrites of the Villa Senni formation. Following this eruption, the complex Tuscolano-Artemisio peri- and extracaldera fissure system, predominantly composed of scoria cones and lavas, formed in response to the deflation of the caldera and peri-caldera area, together with formation of the intracaldera Faete stratovolcano. These edifices were emplaced between c . 355 and c . 180 ka, an interval termed the ‘Tuscolano–Artemisio–Faete period’. Although similar peri-caldera and intracaldera activity occurred earlier, that is, after each major caldera-forming eruption during the Vulcano Laziale period, the Tuscolano–Artemisio–Faete period was subject to a significant reduction in average eruption rate, by one order of magnitude, of 0.1 km 3 ka −1 , which can be related to a consistent reduction in the deep recharging of the plumbing system, and suggesting why no further ignimbrite eruptions occurred after 355 ka. Peri-caldera activity began along the northern and eastern peri-caldera ring fractures (Tuscolano and Artemisio sections, respectively) and after c . 300 ka progressively migrated outwards to extracaldera positions (Pantano Borghese section) and to the western peri-caldera fractures (S. Maria delle Mole section). The activity of these latter fracture systems ended almost simultaneosly, together with that of the Faete intracaldera stratovolcano, between c . 280 and c . 250 ka. After 250 ka, activity migrated to the south (Monte Due Torri section). The most recent activity along this latter peri-caldera area interfingers (between c . 200 ka and c . 180 ka) with phreatomagmatic products, which instead became dominant in the most recent activity of the Colli Albani volcano. Beginning from c . 200 ka (Via dei Laghi period), the western section of the peri-caldera area has been the site of repeated very small- to small-volume, maar-forming phreatomagmatic eruptions, which formed both monogenetic and polygenetic maars, collectively named the Via dei Laghi maar field. The most recent of these maars is the polygenetic Albano maar, which was formed after c . 70 ka by at least seven eruptions migrating along a NW–SE-trending, 3.5-km-long fracture. The last eruption of the maar occurred at <23 ka. Subsequent phreatic activity occurred throughout the Holocene, with lahars originating from dramatic withdrawals of the deep maar lake, at least up to the Eneolithic time (6000–5000 years ago) and probably up to Roman times (fourth century BCE), when the Romans dug a tunnel drain to keep the lake at a constant low level. The Albano area is currently the site of volcanic gas emissions, ground uplift and periodic seismic swarms, which may indicate persistent activity of a magmatic body at depth.