![]() ![]() The first uses etch pits measuring lengths inside the pit. The most quantitative of these are the two methods of Matsuda ( 12). Hence, previous work ( 12– 14) focused on determining grain orientation with respect to the grain boundary. Neighboring grain lattice orientation is a critical issue in the ice-core and glaciology communities ( 11). ![]() Ice is unusual in that the macroscopic sample does not reveal the crystal lattice orientation. It is therefore desirable to prepare macroscopic samples with known faces. In addition, crystallites are perturbed by the supporting surface. ( iii) Small crystallites can be well characterized but, as highlighted by Libbrecht and Rickerby ( 8), results can be clouded by competition from nearby crystallites small faces compete with adjacent faces. However, ice on a substrate often has distinctly different properties from those of neat ice indeed, such ice can even be hydrophobic ( 4, 5)! ( ii) Uptake measurements often use a Knudsen cell with vapor-deposited ice on a substrate ( 6) or compacted, finely divided, artificial snow ( 7) to arrive at a molecular-level picture for gas–particle interaction despite the irregular, highly variable surfaces used. Several strategies have been adopted for studying ice: ( i) Depositing solid water on a metal or ionic substrate that matches the oxygen lattice ( 2, 3). As a result, questions about molecular-level dynamics, surface binding site patterns, and the molecular-level structure remain unanswered ( 1). Applying the single-crystal surface strategy to ice––arguably one of the most fundamental and ubiquitous hydrogen-bonded interfaces––has been limited due to challenges associated with surface generation. Studies of model, single-crystal surfaces have revolutionized understanding of a vast array of heterogeneous catalysts and nanoparticles ranging from pure metals to alloys to semiconductors. ![]()
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