Hexagonal Ice (ice Ih)

Hexagonal ice

There are four different naturally-occurring morphological forms of hexagonal ice; snow, firn (multi-year snow), freshwater ice and sea ice [3584]. Hexagonal ice ([1969], ice Ih ⁱ see Phase Diagram), is in Space group P6₃/mmc, 194; symmetry D_6h, Laue class symmetry 6/mmm; analogous to β-tridymite silica or lonsdaleite, having a six-fold screw axis (rotation around an axis in addition to a translation along the axis). It possesses a relatively open low-density structure, where the packing efficiency is low (≈ 1/3) compared with simple cubic (≈ 1/2) or face-centered cubic (≈ 3/4) structures ^a (and in contrast to face-centered cubic close-packed solid hydrogen sulfide).

 

The crystals may be thought of as consisting of mirror images of corrugated oxygen sheets lying on top of each other. The basic structure consists of a hexameric box where planes consist of chair-form hexamers (the two horizontal planes, opposite) or boat-form hexamers (the three vertical planes, opposite). In contrast, cubic ice contains solely chair-form hexamers. In this diagram, the hydrogen-bonding is shown ordered whereas, in reality, it is random, ^b as protons can move between (ice) water molecules at temperatures above about 5 K [1504]. Indeed, it is likely that the protons in ice behave like a quantum liquid in a constant tunneling flux [2301]. This idea is reinforced by neutron scattering experiments showing a proton scattering density midway between oxygen atoms [1969] indicating proton delocalization and concerted proton movement.

 

The water molecules have a staggered arrangement of hydrogen-bonding with respect to three of their neighbors, in the plane of the chair-form hexamers. The fourth neighbor (shown as vertical links opposite) has an eclipsed arrangement of hydrogen-bonding.

 

Ice crystal structure showing three crystal planes

 

The prism face water molecules extend slightly further (0.39 nm) than the basal plane water molecules (0.37 nm) [3385]

 

 

 

 

Hexagonal ice crystals form hexagonal plates and columns where the top and bottom faces are basal planes {0001} with enthalpy 5.57 µJ ˣ cm^-2 [3019], and the six equivalent side faces are called the (primary) prism faces {1010}^di with enthalpy 5.94 µJ ˣ cm^-2 [3019]. Secondary prism faces {1120} ^dii with enthalpy 6.90 µJ ˣ cm^-2 [3019] may be formed down the planes formed by the sides of the chair structures.

Hexagonal ice shows an anomalous reduction in thermal conductivity with increasing pressure (as do cubic ice and low-density amorphous ice) but different from most crystals. This is due to changes in the hydrogen-bonding decreasing the transverse sound velocity [617]. The experimental 2D IR spectra of D₂O isotopically-pure ice Ih, ice II, ice V, and ice XIII have been compared [3121].

 

Methods have been published describing how to prepare large ice crystal samples and any desired face of ice [3019]. The hydrogen-bonding in the surface of hexagonal ice is predicted to be more ordered than that within the bulk structure [1529]. The X-ray absorption spectra determined for preparations of hexagonal ice, although qualitatively similar, give differences in the values of pre-edge, main-edge and post-edge intensities and their relative ratios. This may be due to different preparation procedures giving possible contamination by cubic ice or low-density amorphous (LDA) ice [3558]..

 

Phase-resolved sum-frequency-generation vibrational spectroscopy has shown that there is a structural asymmetry between the top two layers (L1 top layer of water hexagons, L2 second layer of water hexagons) in the subsurface hydrogen-bonding of the basal face of hexagonal ice. Accepted hydrogen bonds in the top surface hexagons (L1 O···H-O L2) are stronger than the accepted hydrogen bonds in the second layer hexagons to the top layer (L1 O-H···O L2) [3100].

 

The electric properties of ice (e.g., electral conductivity) have been explained using the two types of free-moving defects in ice; the presence of ions (H₃O⁺ and OH^-) and Bjerrum defects (wrongly oriented water molecules) [3691]. The structural mechanisms of ice deformation have been studied [3158].

Interactive structures of hexagonal ice (Jmol) are available. [Back to Top ]

Ice nucleation and growth

A recent review covers the progress in ice nucleation [3492]. In the atmosphere, ice-nucleating particles are often naturally mixed with a soluble material. Small concentrations of solutes (0.015 M), with minimal predicted colligative effect (freezing point depression < 0.1 °C) and negligible impact on water activity, can influence the heterogeneous nucleated freezing using suspended particles of feldspars or quartz. Surprisingly the freezing points may be increased by up to 3 °C (using ammonium salts) or decreased (using alkali metal halides) by up to 8 °C for the same nucleating rock particles [3379], with these temperature changes relative to the nucleation without any solute present. Crystallization from supercooled liquid water involves ordering of the molecules and the adoption of their ice lattice positions. The ice nuclei originate within immobile regions of the supercooled water [3523].

 

The minimum number of water molecules necessary for ice nucleation in pure water was originally stated to be the same (i.e., 275±25) as that required for a complete icosahedral cluster (i.e., 280) [1931]. More recent work has suggested that only about 90 molecules are necessary [3801], with water clusters with less than ~ 150 molecules oscillating between the liquid and crystalline (a mixture of structurally similar ice Ih and Ic species) states. Ice nucleation occurs greatly enhanced, by a factor of 10¹⁰, at the air-water surface rather than within bulk water [914]. Ice crystal growth depends on the different rates of growth on each facet with facet nucleation rates dependent on their different step energies. The secondary-prism face is most stable, followed by the primary-prism face and then the hexagonal basal face [2193]. This gives rise to the hexagonal 'snowflake' shapes (see top of page, right), with their great variety due to crystal defects. The physical dynamics of ice crystal growth has been comprehensively described [3019]. Ice nucleation may be triggered by negative pressures such that occurs locally and briefly when water is stretched due to mechanical shock or ultrasonic waves [3123]. Ice nucleation in atmospheric clouds may be through the stacking-disordered ice.

 

Water must be prevented from freezing when cryopreserving biological samples, food, and organs [2853]. This is generally achieved by fast cooling rates, use of small samples and cryopreservation agent, and increasing pressure to beat ice nucleation and avoid cell damage [2821]. The ice/liquid interfacial free energy increases from ≈ 30 mJ ˣ m^-2 at ambient pressure to 40 mJ ˣ m^-2 at 200 MPa indicating the reason for the reduction of the ice nucleation with increasing pressure [2821].

 

Hexagonal ice crystals may form by (slowly) growing in the direction of the c-axis (S1 ice) as inside vertical freezing pipes or where ice crystals grow down vertically from crystal platelets nucleated on still water with their c-axes vertical, and where sideways growth is prevented but axial growth allowed. Alternatively, they may grow more rapidly from the prism faces (S2 ice), as at the disturbed randomly-directed surface of rapidly freezing or agitated lakes. Growth from the {1 1 -2 0} faces is at least as fast as that from the prism faces, but such growth turns these faces into prism faces [827]. Ice crystal growth data has been critically examined [3046]. The relative speeds of this crystal growth, of the different faces, depend on the ability of these faces to form greater extents of cooperative hydration. The temperature of the (supercooled) surrounding water determines the degree of branching in the ice crystal. Crystal growth is limited by the rate of diffusion at a low degree of supercooling (i.e., < 2 °C; giving rise to more branching) but limited by the kinetics of growth at higher degrees of supercooling (i.e., > 4 °C; giving rise to needle-like growth) [883]. The hexagonal crystal structure, the different growth characteristics of the crystal faces and the temperature of the surrounding (supercooled) water are behind the flat six-pointed shapes of snowflakes [1916].

 

The vapor pressure of ice is shown right [IAPWS]. Ice nucleation in the atmosphere profoundly affects cloud formation and properties. Feldspars, found in desert dust that enters the atmosphere by the million tons a year, are important nucleation agents. Computer simulations have indicated that this is due to the nucleation of the prismatic crystal planes of ice on the high-energy (100) surface planes of feldspar [2863].

 

Solutes (except for the very small helium [2204] and hydrogen [2205] molecules that can fit into the interstitial sites) cannot be incorporated into the ice Ih structure at ambient pressure ^f but are expelled to the surface or the amorphous ice layer between the microcrystalline ice crystals [3838]. This may be made use of when purifying water (for example, degassing or desalination [2851] ) using successive freeze-thaw cycles. Some solutes (for example, chaotropic ions such as NH₄⁺ and Cl^-) are incorporated more easily into freezing ice than others (for example, kosmotropic ions such as Na⁺ and SO₄^2-), so removing them from the remaining thin films of liquid between the crystals. This may result in the electrical charging of the surface due to surface water dissociation balancing the remaining charges (which also may give rise to electromagnetic emission) and changes in the pH of the residual liquid films (for example, (NH₄)₂SO₄ becomes more acidic [1010], and NaCl becomes more alkaline [1089]). The concentration of salts in aqueous channels, between the pure ice particles, gives rise to efficient ionic transport and the ice becoming an apparently solid-state ionic conductor [3755].

 

Views perpendicular to the faces of the ice (1h) crystal showing the next layer attached (with O-atoms black). (a) Slow growing basal {0 0 0 1} face (viewing down the c-axis); where only isolated water molecules attach. (b) faster growing {1 0 -1 0} prism face (viewing down the a-axis), where pairs of newly-attached water molecules may hydrogen bond to each other; one hydrogen bond/two water molecules. (c) Fastest growing {1 1 -2 0} (secondary prism) face, where chains of newly-attached water molecules may cooperatively hydrogen bond to each other; one hydrogen bond/water molecule. These form ridges which divide and encourage conversion into two prism faces. The radial distribution functions are shown elsewhere.

 

The development of icephobic surfaces is very important for transportation systems (e.g. plane wings), power systems (e.g. power cables), and energy systems (e.g. electricity transmission). Icephobic surfaces should have low freezing temperature, low ice accretion rate, low ice adhesion, and long-term durability [3611].

 

The freezing of water in soap bubbles is different from that in liquid water with many ce crystals growing iat the same time and swirling around the bubbles [3677].

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Zero-point entropy

The zero-point entropy may be defined as

 

S₀ = k_B ˣ Ln(N_E0)

 

where k_B is the Boltzmann constant, N_E is the number of configurations at energy E, and E0 is the lowest energy. This value for the entropy of hexagonal ice at zero kelvin does not break the third law of thermodynamics "The entropy of a perfect crystal at absolute zero is exactly equal to zero" as the hexagonal ice crystals are not perfect, having disordered hydrogen-bonding.

 

In hexagonal ice, the hydrogen-bonding is random and rapidly changing (while obeying the 'ice rules'). These structures are not precisely equal in energy but spread out over a very large number of energetically close states. The zero-point entropy is entropy (disorder) that would remain even if the material could be cooled to absolute zero ( 0 K = −273.15 °C). This disorder gives rise to an experimental zero-point entropy for hexagonal ice of 3.41 (± 0.2) J ˣ mol^-1 ˣ K^-1.

 

Theoretically, it should be possible to calculate the zero-point entropy of the known ice crystals with far more accuracy (neglecting flaws, defects and the spread of energy levels) than determining it experimentally. However, their exact calculation has been found to be in need of cleverer mathematicians than having, so far, tackled the problem.

 

Linus Pauling made an estimate of the number of hydrogen-bonded configurations of ice = R ˣ Ln(3/2) = 3.371 J ˣ mol^-1 ˣ K^-1 (0.99 ˣ the experimental value and the lower bound of the exact value). Pauling used the number of configurations equaling (6 ˣ ¼)^N, where N is the number of molecules. The (6 ˣ ) term is due to there being six possible arrangements of the hydrogen atoms along the four hydrogen bonds around each oxygen atom (1&2, 1&3, 1&4, 2&3, 2&4, 3&4, see right). The ( ˣ ¼) term is due to two of the four bonds connecting the oxygen to its four neighbors are already occupied by their neighbors' protons, and the probability, that a particular bond does not already have a hydrogen atom on it, is one-half. The probability that two selected bonds are both free of protons is (½ ˣ ½) = (¼).

 

Pauling's estimate makes no allowance for the many correlations introduced from the closed hydrogen-bonded loops. The rationale is that the chances of a bond being allowed in a ring of hydrogen bonds are slightly greater than ½ as the linkages are correlated. The hydrogen bond being donated from the last water molecule in the ring of water molecules to the first molecule in that ring finds a water molecule that has 2/3 free space rather than 2/4. Thus the (½ ˣ ½) term is an underestimate, and Pauling's estimate is low; see [717] for further discussion of this point. A better estimate of the zero-point entropy, from averaging multiple simulations, is R ˣ Ln(1.507117) = 3.413 J ˣ mol^-1 ˣ K^-1 [1090]; about 1% higher.

 

Although the proton order in bulk ice is disordered, the surface of the ice probably has a preference for proton order in terms of stripes of dangling H-atoms and O-lone pairs [1551]. The zero-point entropy of ices with ordered hydrogen bonds (such as ice-two) is zero. The zero-point entropies (ZPE, J ˣ mol^-1 ˣ K^-1) of other ices have been found [3107] to be

 

Order          Ih   =    Ic   =  Ice VII <  Ice III  < Clathrate I < Clathrate II < Ice V < Clathrate H < Ice VI
ZPE	3.41251	3.41251	3.41251	3.41975	3.43191	3.43285	3.43433	3.43834	3.50082
Ratio %	100.00	100.00	100.00	100.21	100.57	100.60	100.64	100.76	102.59

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Footnotes

^a   The exact packing efficiency for ice Ih is low

≈ ≈ 0.34,            ≈ 1/3

compared with the simple cubic

                           = 0.5236,                     ≈ 1/2

 

or the body-centered cubic

                      = 0.6802,                      ≈ 2/3

 

or the face-centered cubic and hexagonal close packed

                 = 0.7408,                      ≈ 3/4

structures [811]. [Back]

 

^b  In all these structural diagrams the hydrogen-bonding is ordered whereas, in reality, it is random and rapidly changing (obeying the 'ice rules'). As the H-O-H angles are about 106.6º [717], the hydrogen bonds are not straight (although shown so in the figures). Although each water molecule is shown symmetrically situated, thermal motion causes a broad range of the hydrogen bond energies giving noticeable instantaneous asymmetry around the crystallographic sites [2095]. [Back]

 

^d  (i) There are six prism face planes around the hexagonal crystal; going anticlockwise {0 1 -1 0} {-1 1 0 0} {-1 0 1 0} {0 -1 1 0} {1 -1 0 0} {1 0 -1 0}. (ii) There are six such secondary prism face planes across similar diagonals in the hexagonal crystal; going anticlockwise {1 1 -2 0} {-1 2 -1 0} {-2 1 1 0} {-1 -1 2 0} {1 -2 1 0} {2 -1 -1 0}. [Back]

 

^f   However, the close match of the crystal lattice constants between hexagonal ice and hexagonal β-AgI makes the AgI an effective ice nucleating agent [2833]. Similarly, the hydrogen-bonded salt NH₄F (with both NH₄⁺ and F^- being of similar size to H₂O molecules and giving tetrahedrally directed hydrogen bonds, with hexagonal unit cell dimensions 4.37 Å (a) and 7.17 Å (c)) can also form thoroughly mixed hexagonal crystals [1568]. The poor solubility of other solutes in hexagonal ice does not extend to the high-pressure ices, where salts may be incorporated into the crystal lattice. [Back]

 

^g   There seems to be an error in the published equation, where the denominator is given as 273.15. [Back]

 

^h  The variation of some physical properties of ice may be given in terms of the temperature (T, °C) [1665]:

Density of ice (kg m^-3) = 917 – 0.13 ˣ T

Specific heat of ice (kJ kg^-1 K^-1) = 2.12 + 0.008 ˣ T

Thermal conductivity of ice (W m^-1 K^-1) = 2.21 – 0.012 ˣ T

Enthalpy of ice (kJ kg^-1) = –332.4 + T (2.12+0.008 ˣ T)

 

Note that ice often has included gas pockets within its structure and hence has an apparently lower density and altered physical properties.

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ⁱ   The I in 'ice Ih' is the Roman numeral for one, as this was the first water ice found. [Back]