readers. Silica (SiO2) is the most abundant component of rocks, and the common extrusive rocks are classified into silica‐rich (felsic) rocks and silica‐poor (mafic) rocks. Ice or the solid state of water (H2O) is crystalline and belongs to the hexagonal system in Earth's crust; however, individual ice crystals are extremely pure because ice lattice is very intolerant to inclusions. Water, of course, is a liquid with amorphous structure, but oceans in the Arctic and Antarctic regions can be “ice rich” (often described for wrong reasons as “ice‐infested”), depending on the season.
Interestingly, viscous molten rocks or magma at extremely high temperatures at great depths below Earth's surface could be similar in behavior to ice‐rich water (specially with thick layers containing frazil ice crystals) on Earth's crust. The structure and fluidity of magma depends on location, depth, and temperature. As temperature and pressure decrease with decrease in depth, the viscosity of magma and its constitution change. The viscosity of the mass depends on its structure, because different types of crystals form depending on the eutectic points and float, separated or trapped within the melt, and are extruded if possible. Structural features of magma are very complex simply because of pressure, thermal state, and different mineral contents with wide‐ranging concentrations. It is impossible to conduct in situ studies of magma, but laboratory investigations are often performed on quenched melts or glasses of simple compositions as analogs (Henderson et al. 2006; Greaves and Sen 2007).
1.3.1 Ice: A High‐Temperature Material
Geophysicists or solid‐earth scientists can only make educated guesses about what sort of molten rocks are in magma of the mantle, but glacier physicists, as declared by Weertman and Weertman (1975), know that the bulk of their glacial material is rather pure ice (consolidated snow) and its in situ thermal state. They can obtain samples by deep drilling for cores in glaciers, ice sheets, ice caps, and ice shelves and concurrently measure borehole temperature distribution. Rather sophisticated understanding of the flow of large ice masses was also developed primarily based on unconfined, uniaxial laboratory creep tests on glacial ice in wide ranges of stress and temperature (Liboutry 1965; Paterson 1994). Microstructural investigations were also carried out including the role of dislocation dynamics. Most importantly, ice was recognized as a high‐temperature polycrystalline material. The physics of glaciology encompassing the mechanics of glaciers, ice caps, etc. was formulated theoretically on experimental observations that polycrystalline ice obeyed power‐law creep (primarily dislocation creep) for secondary or steady‐state flow, experimentally obtained from the stress dependence of the minimum creep rate (mcr),
Even though the word glaciology truly stands for the study of ice in all its phases and conditions, sadly the subject of glaciology generally implies the study of glaciers. Popular dictionaries even define glaciology as “the study of the distribution, character, and effects of glaciers” (Simpson and Weiner 1989). This definition has certainly been expanded over the years to include large ice masses, such as ice sheets and ice shelves. Glaciological sciences are becoming increasingly important in the twenty‐first century with current international attention on climate change (popularized as “global warming”) and environment impacts due to increasing pollution of air and water bodies. Melting of glaciers, ice sheets, and ice shelves with concomitant rising of sea level, surface temperature of the oceans, and decrease in the extent of sea ice covers are some of the issues of importance. As such, the studies related to the physics of glaciers and ice are receiving a renewed interest. Accordingly, Paterson (1994) revised his original 1969 book (second edition in 1981) completely, “in order to keep pace with the extensive developments since the second edition was published.” No doubt, Paterson (1994) performed a formidable task, saying, “The vast expansion of the literature in recent years is making it increasingly difficult for one person to write a comprehensive account of the physics of glaciers.” The dictionary definition of “glaciology” has, however, remained unchanged; the physics and mechanics of ice has remained within the framework related to slow movements of large ice masses of glacial origin. The compaction of porous snow to nonpermeable ice and the long‐term flow of the mass in terms of secondary and tertiary stages of dislocation/diffusion creep over the range of stresses important in normal glacier flow (50–200 kPa or 5 × 10−6E to 2 × 10−5E, where E is the Young's modulus of ice) remained the focus (Paterson 1994).
Glaciologists devoted to understanding the long‐term response of glaciers or ice sheets and their environmental impacts, such as sea level rise, have had no requirements for understanding strength‐related mechanical properties of ice. However, ice–structure interactions (including off‐shore structures), bearing capacity of floating ice covers or winter roads used for transportation, building materials and roads subjected to freezing and thawing, permafrost‐related issues, etc. are some of the many ice engineering problems. In all of these types of ice engineering problems, knowledge of transient (primary) creep of ice and micromechanics of deformation, nucleation, and kinetics of cracking is essential. Naturally, ice engineers looked toward glaciological literature for their inputs. However, glaciologists were influenced by ideas developed for long‐term flow of glaciers on the basis of steady‐state flow. They concentrated their efforts toward the use of “mcr,”
Realizing the ice engineering issues, the senior author looked at materials science interconnected to very short‐term (early transient) creep of polycrystalline metals and alloys when he started his career in physics and mechanics of ice in 1975. He noticed that since the pioneering work of da Costa Andrade (1910) on steel, materials scientists paid only a “passing interest” in transient or the decreasing primary creep regime. Efforts were concentrated mainly on secondary, steady‐state, or strictly speaking minimum creep rate (Norton 1929; Nadai 1938; Glen 1955; Garofalo 1965; Odqvist 1974; Gittus 1975; Evans and Wilshire 1985; Cadek 1988; Nabarro and de Villiers 1995; Kassner 2015, etc.). However, creep failures either by fracture or necking depend on stress and temperature. Ruptures tend to occur near the end of the primary creep approaching the secondary stage and most certainly during the accelerating or tertiary regimes. Similar to the primary creep, historically, little attention has been paid to tertiary stages until recently. Yet, innumerable studies have been performed in characterizing the secondary creep or strictly speaking minimum creep rate, of various materials. To reduce effort and time, most studies are being performed at relatively high stresses to attain well‐defined minimum creep rates in reasonable lengths of time.
The European
