Biogenic Orthorhombic α-Calcium Formate from Sediments of Alkali Lake, Oregon, USA

Abstract

Centimeter-sized crystals of orthorhombic calcium formate, α-Ca(HCO₂)₂ from Alkali Lake, Oregon, USA have been studied by means of powder and single-crystal X-ray diffraction analysis, infrared, and Raman spectroscopy. Based on the data on carbon isotope abundance in calcium formate and associated minerals, it was concluded that the formation of α-Ca(HCO₂)₂ may be a result of a combination of two factors: lake microbial metabolism and anthropogenic pollution with Agent Orange. Possible causes of stability of the low-density tetragonal β-Ca(HCO₂)₂ polymorph (formicaite) in boron ores are discussed.

1. Introduction

Crystalline formates are rare in nature. There are only two species belonging to this class of minerals: formicaite Ca(HCO₂)₂ [1] and dashkovaite Mg(HCO₂)₂·2H₂O [2]. Both formate minerals were discovered in Russia. They were found in low-temperature hydrothermal veinlets in three boron-rich skarn deposits, namely Solongo, Buryatia, Siberia, Novofrolovskoe, Northern Urals (formicaite), and Korshunovskoe, the Irkutsk district, Siberia (dashkovaite). Later, trace amounts of these minerals have been detected by us in boron-bearing metasomatic parageneses of some other deposits by means of IR spectroscopy which was found to be an effective tool to detect small amounts of the formate minerals. Using this method, we also detected admixtures of unidentified formates in sediments of saline lakes of California, USA. Thus, the confinement of formates to areas bearing boron mineralization is a reliably established fact.

There are four polymorphic modifications (α–δ) of synthetic anhydrous calcium formate known nowadays (

Table 1. Crystallographic data for Ca(HCO₂)₂ polymorphic modifications.

Modification	Sp. Gr.*	a, Å/α, °	b, Å/β, °	c, Å/γ, °	V, Å3/ ρ, g/cm3	Reference
α	Pbca	10.229(1)	6.256(1)	13.243(1)	847.47(2)/2.040	This work
		10.163–10.228(3)	6.261(3)–6.288(1)	13.238(5)–13.407(2)	847.73–858.81/2.008– 2.038	[6,7,8,9,10]
β (synt)	P41212	6.776(2)	6.776(2)	9.453(5)	434.03/1.991	[5]
β (Formicaite)		6.77(1)	6.77(1)	9.46(1)	434(1)/1.990	[1]
γ	P2, Pm or P2/m	6.75/90	6.705/119.47	5.78/90	227.75/1.897	[4]
δ	I41/amd	6.75(1)	6.75(1)	10.04(2)	457.45/1.889	[5]

* Crystallographic data for α-Ca(HCO₂)₂ are given in a uniform setting. However, various settings of the same unit cell and isomorphic space groups (Pbca or Pcab) can be found in original works.

) [3,4]. Orthorhombic α- and tetragonal β-Ca(HCO₂)₂ can persist at ambient conditions, while γ- and δ-modifications are transition phases and can exist in a high-temperature range of 150–300 °C [4]. Besides, both α- and β-modifications transform directly to γ- and then to δ-modification upon heating (α → γ → δ and β → γ → δ), and there is no α → β transformation detected to date, while a series of phase transitions at cooling include all modifications: δ → γ → β → α. Among them, α-Ca(HCO₂)₂ is supposed to be the most stable, since the β-modification easily transforms to the orthorhombic α-modification at room temperature in a humid atmosphere [5]. It should be noted that the crystal structure of γ-Ca(HCO₂)₂ is still not determined, and indexation of its powder pattern in a monoclinic unit cell leaves some doubts due to the rather rare tendency of symmetry reduction with heating.

Formicaite, the tetragonal β-modification of Ca(HCO₂)₂, was the first natural salt of formic acid approved by the International Mineralogical Association as a mineral species. The orthorhombic calcium formate polymorph, α-Ca(HCO₂)₂, is known as a synthetic phase, which among the other pathways, can be obtained by evaporation of a calcite solution in formic acid [11].

In this paper, we describe orthorhombic calcium formate from sediments of highly saline, and alkaline Alkali Lake, Oregon, USA. Orthorhombic α-Ca(HCO₂)₂ occurs there as aggregates of colorless, flattened crystals up to 5 mm across (Figure 1).

2. Materials and Methods

Centimeter-sized crystals (Figure 1a) of orthorhombic α-Ca(HCO₂)₂ were obtained from the lacustrine sediments of Alkali Lake, Valley Falls, Lake Co., Lake County, OR, USA.

In order to obtain IR absorption spectra, powder samples of orthorhombic α-Ca formate and formicaite (used for comparison) were mixed with anhydrous KBr, pelletized, and analyzed using an ALPHA FTIR spectrometer (Bruker Optics; Ettlingen, Germany) at a resolution of 4 cm⁻¹. A total of 16 scans were collected. The IR spectrum of an analogous pellet of pure KBr was used as a reference.

Raman spectra were obtained on randomly oriented samples using an EnSpectr R532 (EnSpectr, Chernogolovka, Russia) instrument (calibrated using the 520 cm⁻¹ band of Si) with a green laser (the exciting wavelength λ = 532 nm) at room temperature. The output power of the laser beam was about 14 mW. The spectrum was processed using the EnSpectr expert mode program in the range from 100 to 4000 cm⁻¹ with the use of a holographic diffraction grating with 1800 lines/cm; a resolution was about 6 cm⁻¹. The diameter of the focal spot on the sample was about 10–12 μm. The backscattered Raman signal was collected with a 40× objective the signal acquisition time for a single scan of the spectral range was 1 s and the signals were averaged over 100 scans for orthorhombic Ca-formate and over 50 scans for formicaite.

Powder X-ray diffraction (PXRD) data were collected with a STOE Stadi MP (STOE, Darmstadt, Germany) powder diffractometer operated with monochromated (curved Ge(111)) CoKα₁ radiation (λ(CoKα₁) = 1.78896 Å) at 45 kV and 35 mA using transmission geometry with a scan step of 0.02°. PXRD data was processed using STOE WinXPOW software [12].

Single crystal X-ray diffraction (SCXRD) studies were carried out at 100 K using a Rigaku Oxford Diffraction XtaLab SuperNova diffractometer (Rigaku Oxford Diffraction, Oxford, UK) equipped with a hybrid photon counting HyPix-3000 detector operated with monochromated, microfocused CuKα radiation (λ(CuKα) = 1.54184 Å) at 50 kV and 0.8 mA. Data were integrated and corrected for background, Lorentz, and polarization effects. An empirical absorption correction based on spherical harmonics implemented in the SCALE3 ABSPACK algorithm was applied in the CrysAlisPro program [13]. The unit-cell parameters (

Table 2. Crystallographic data for α-Ca(HCO₂)₂ from Alkali Lake.

Crystal System	Orthorhombic
Space group	Pbca
a (Å)	10.22943(12)
b (Å)	6.25587(9)
c (Å)	13.24297(18)
V (Å3)	847.471(19)
Molecular weight	130.12
μ (mm–1)	11.986
Temperature (K)	100(2)
Z	8
Dcalc (g/cm3)	2.040
Crystal size (mm3)	0.16 × 0.11 × 0.08
Radiation	CuKα
Total reflections	6597
Unique reflections	806
Angle range 2θ (°)	13.37–140.00
Reflections with |Fo| ≥ 4σF	802
Rint	0.0461
Rσ	0.0188
R1 (|Fo| ≥ 4σF)	0.0195
wR2 (|Fo| ≥ 4σF)	0.0542
R1 (all data)	0.0195
wR2 (all data)	0.0542
S	1.090
ρmin, ρmax, e/Å3	−0.296, 0.408
CSD	2070226

R₁ = Σ||F_o| − |F_c||/Σ|F_o|; wR₂ = {Σ[w(F_o² − F_c²)²]/Σ[w(F_o²)²]}^1/2; w =1/[σ²(F_o²) + (aP)² + bP], where P = (F_o² + 2F_c²)/3; s = {Σ[w(F_o² − F_c²)]/(n − p)}^1/2 where n is the number of reflections and p is the number of refinement parameters.

) were refined using the least-squares techniques. The structure was solved by a dual-space algorithm and refined using the SHELX programs [14,15] incorporated in the OLEX2 program package [16]. The final model included coordinates and anisotropic displacement parameters for all non-H atoms (

Table 3. Atomic coordinates and isotropic displacement parameters (Ų) for α-Ca(HCO₂)₂ from Alkali Lake.

Atom	x	y	z	Ueq
Ca1	0.63497(2)	0.46904(4)	0.60687(2)	0.00687(15)
O1	0.47731(8)	0.28344(15)	0.70119(7)	0.0118(2)
O2	0.29850(8)	0.28148(15)	0.79756(7)	0.0104(2)
O3	0.79847(8)	0.63126(15)	0.51242(7)	0.0131(2)
O4	0.96604(8)	0.80824(15)	0.45160(7)	0.0125(2)
C1	0.37446(11)	0.3653(2)	0.73323(10)	0.0091(3)
H1	0.3486(15)	0.503(3)	0.7099(14)	0.014(4)
C2	0.88857(12)	0.6535(2)	0.44933(10)	0.0102(3)
H2	0.9009(18)	0.547(3)	0.3972(12)	0.012(4)

). The carbon-bound H atoms were localized from different Fourier maps and were included in the refinement without any restraints with individual isotropic displacement parameters. Supplementary crystallographic data were deposited in the Inorganic Crystal Structure Database (ICSD) and can be obtained by quoting the CSD 2070226 via www.ccdc.cam.ac.uk/structures/ (see Supplementary Materials).

3. Results

3.1. Infrared Absorption Spectroscopy

The bands of fundamental modes in the IR spectra of orthorhombic α-Ca formate and formicaite (Figure 2) were observed in the following ranges: 2870–2900 cm⁻¹ (C–H stretching vibrations); 1580–1660 cm⁻¹ (antisymmetric stretching vibrations of the –CO₂ carboxylate group); 1350–1400 cm⁻¹ (symmetric stretching vibrations of the –CO₂ group combined with O–C–H bending vibrations); and 780–810 cm^–1 (bending vibrations of the –CO₂ group combined with O–C–H bending vibrations). Weak bands in the ranges 2690–2780 and 2940–3010 cm⁻¹ corresponded to overtones and combination modes, respectively.

The presence of single bands at 789, 1605, and 2874 cm⁻¹ in the IR spectrum of formicaite was in agreement with the presence of the only type of the formate anions in the crystal structure of α-Ca(HCO₂)₂. The doublet 1362 + 1380 cm⁻¹ was related to the mixed modes involving in-plane and out-of-plane O–C–H bending vibrations combined with symmetric stretching vibrations of the carboxylate group.

In the IR spectrum of orthorhombic α-Ca formate, each fundamental band was split into two components which reflected the presence of two nonequivalent formate anions in the crystal structure of α-Ca(HCO₂)₂ (Section 3.3). Additional splitting of the band of antisymmetric stretching vibrations of the carboxylate group may be due to Fermi resonance with an overtone of the combined O–C–H and O–C–O bending vibrations.

3.2. Raman Spectroscopy

The Raman spectra of α- and β-modifications of Ca(HCO₂)₂ are presented in Figure 3. The assignment of the Raman bands is as follows [17,18]:

• 2870 to 2890 cm⁻¹, C–H stretching vibrations;
• 1573 to 1600 cm⁻¹, antisymmetric stretching vibrations of the –CO₂ group;
• 1353 to 1387 cm⁻¹, symmetric stretching vibrations of the –CO₂ group;
• 1069 cm⁻¹, in-plane H–C–O bending mode;
• 754 to 800 cm⁻¹, bending vibrations of the –CO₂ group combined with O–C–H bending vibrations;
• 213 and 233 cm⁻¹, stretching vibrations involving Ca···O ionic bonds.

The bands in the range of 390–550 cm⁻¹ observed in the Raman spectrum of formicaite were due to unidentified impurities. Other weak bands in the Raman spectra of α- and β-Ca(HCO₂)₂ corresponded to overtones and combination modes.

The band of Ca···O stretching vibrations in the Raman spectrum of α-Ca(HCO₂)₂ (at 233 cm⁻¹) shifted towards higher frequencies as compared to the analogous band of β-Ca(HCO₂)₂ observed at 213 cm⁻¹. This phenomenon is related to the differences in the coordination of Ca in the structures of these polymorphs, the coordination numbers of Ca being equal to 7 in α-Ca(HCO₂)₂ and 8 in β-Ca(HCO₂)₂.

3.3. X-ray Diffraction Data and Crystal Structure

The crystal structure of α-Ca formate was first described in the late 1940s [6]. Then, it was re-determined several times in the 1970s and 1980s [7,8,9,10] in various settings of the same orthorhombic unit cell (Table 1) and isomorphic space groups (Pbca or Pcab). The most recent refinement preceding our work was reported by Wang et al. [19].

There was one crystallographically non-equivalent Ca atom in the structure of α-Ca(HCOO)₂ which was coordinated by seven O atoms of two unique formate groups (Figure 4a) to form a distorted pentagonal bipyramid as a coordination polyhedron. Six formate groups were involved in the coordination; only one of them was bidentate, acting as a chelate ligand, while the other five groups were linked to the Ca atom in a monodentate manner. Ca-centered polyhedra shared edges with the adjacent distorted bipyramids to form dioctahedral-like layers (Figure 4b) that were arranged parallel to (001) and were linked in a framework structure via bridging formate groups (Figure 4c). It should be noted that in some of the previous works, coordination of Ca-centered polyhedra was described as an 8- or (7 + 1)-fold with one long contact Ca1···O1 = 3.413(1) Å. However, this contact is highly doubtful, because even the Ca1···C distances are shorter (3.213(1) and 2.882(1) Å for C1 and C2, respectively), and the 7-fold geometry satisfies bond-valence sums (

Table 4. Selected bond lengths (Å), angles (°), and bond-valence sums (BVS, in valence units (v.u.)) in the crystal structure of α-Ca(HCO₂)₂ from Alkali Lake.

Bond *		BVS	Angle
Ca1–O1	2.3472(9)	0.341	O1–Ca1–O4	87.42(3)
Ca1–O2	2.4036(9)	0.297	O1–Ca1–O4	87.90(3)
Ca1–O2	2.4260(9)	0.281	O2–Ca1–O2	85.60(2)
Ca1–O3	2.5482(10)	0.209	O2–Ca1–O3	70.59(3)
Ca1–O3	2.3220(9)	0.363	O2–Ca1–O3	148.13(3)
Ca1–O4	2.3510(9)	0.338	O2–Ca1–O4	121.46(3)
Ca1–O4	2.5115(9)	0.228	O2–Ca1–O4	149.91(3)
<Ca1–O>	2.416	2.057	O3–Ca1–O1	176.17(3)
Ca1···O1 **	3.413(1)	0.025	O3–Ca1–O2	74.15(3)
			O3–Ca1–O2	89.75(3)
C1–O1	1.2447(15)		O3–Ca1–O3	84.58(3)
C1–O2	1.2667(15)		O3–Ca1–O4	91.74(3)
C1–H1	0.952(19)		O3–Ca1–O4	95.34(3)
C2–O3	1.2518(16)		O4–Ca1–O2	84.29(3)
C2–O4	1.2512(17)		O4–Ca1–O2	166.99(3)
C2–H2	0.969(17)		O4–Ca1–O3	51.39(3)
			O4–Ca1–O3	121.75(3)
Angle			O4–Ca1–O4	70.45(4)
O1–Ca1–O2	108.28(3)		O1–C1–O2	125.26(13)
O1–Ca1–O2	87.51(3)		O3–C2–O4	122.44(13)
O1–Ca1–O3	91.98(3)

* Bond-valence sums were calculated using [20]. ** Contact is not included in the coordination sphere of Ca atom; see text for details.

).

In contrast to α-Ca(HCOO)₂, in which all atoms occupy general sites, the crystal structure of the tetragonal β-modification (formicaite) contained one unique Ca atom-occupying special site on a 2-fold axis, and one unique formate anion, all atoms of which occupy general sites. The Ca atom is coordinated by eight O atoms that belong to two trans arranged chelating bidentate formate groups and four monodentate formate ligands. The coordination polyhedron of Ca atom in the structure of β-Ca(HCOO)₂ can also be described as a distorted pentagonal bipyramid, in which four equatorial O atoms are arranged as in regular pentagonal bipyramid, and the fifth vertex is split into two sites that belong to the second chelating formate molecule and occur above and below the mean equatorial plane (Figure 4d). The average <Ca–O> distance in the structure of β-Ca(HCOO)₂ was equal to 2.526 Å and was larger than that for α-Ca(HCOO)₂, which was due to the 8-fold coordination and XRD data collection at room temperature [5]. On the other hand, the BVS parameters for Ca atoms in the structures of both α- (2.057 v.u.) and β-modifications (2.044 v.u.) were comparable. In β-Ca(HCOO)₂, the Ca-centered polyhedra shared edges with the adjacent complexes to form dioctahedral-like layers (Figure 4e) that were arranged parallel to (101) and equivalent planes perpendicular to the 4₁-fold axis. Unlike the structure of α-Ca(HCOO)₂, these layers in β-Ca(HCOO)₂ were interlinked with each other directly, without spaces, by sharing edges of Ca polyhedra (Figure 4f).

The powder diffraction pattern fits very well with the calculated from the structural data of α-Ca(HCO₂)₂ from the Alkali Lake reported herein (

Table 5. Powder X-ray diffraction data (d in Å) for α-Ca(HCO₂)₂ from Alkali Lake.

dmeas	Imeas	Icalc	dcalc	hkl	dmeas	Imeas	Icalc	dcalc	hkl
6.692	5	7	6.656	002			4	1.922	511
5.596	100	100	5.577	102	1.916	11	13	1.917	231
4.965	60	57	4.963	111	1.865	9	14	1.859	306
3.952	2	3	3.962	210			3	1.812	026
3.793	15	18	3.798	211	1.807	1	4	1.809	423
3.426	20	18	3.415	113	1.791	5	7	1.784	126
3.406	96	94	3.405	212			2	1.782	316
3.058	21	21	3.056	021			3	1.775	233
2.961	87	82	2.955	213	1.767	11	19	1.767	331
2.928	4	3	2.927	121			2	1.746	134
		3	2.920	311	1.722	9	6	1.722	332
2.839	23	7	2.839	022			11	1.714	217
		29	2.826	114	1.704	3	2	1.703	600
2.739	15	18	2.736	122			5	1.702	424
2.674	3	4	2.675	220	1.678	5	6	1.675	406
		4	2.554	400			2	1.674	234
2.546	4	2	2.548	214	1.655	1	4	1.658	522
2.490	12	13	2.486	123			2	1.642	108
2.483	15	14	2.481	313	1.632	1	4	1.631	611
		12	2.383	115	1.627	4	2	1.627	027
2.291	20	24	2.284	024			5	1.624	135
2.272	1	3	2.274	321	1.598	3	4	1.595	612
2.234	16	12	2.229	124	1.591	2	2	1.589	425
2.229	19	20	2.225	314			3	1.589	118
2.218	4	2	2.219	006			2	1.582	208
		3	2.210	215			2	1.541	141
2.180	17	19	2.181	322	1.538	5	11	1.541	613
		3	2.168	106	1.511	2	4	1.511	142
		2	2.048	323	1.480	2	5	1.480	043
2.026	11	2	2.027	131			2	1.478	426
2.001	2	10	2.026	404			5	1.470	028
1.994	16	6	1.992	125	1.421	2	3	1.426	119
		22	1.989	315			3	1.420	044
1.978	13	19	1.981	420	1.409	1	6	1.413	711
		5	1.960	132	1.398	1	3	1.394	408
1.948	8	12	1.953	502	1.358	2	4	1.357	237
1.936	4	6	1.937	230			6	1.356	526

). A calculated pattern was obtained using atomic coordinates generated from structural refinement and unit cell parameters refined from the powder pattern: a = 10.215(3); b = 6.2787(15); c = 13.312(5) Å; V = 853.8(3) ų.

4. Discussion

An interaction of biogenic and abiogenic systems in nature and in laboratory conditions quite often leads to the formation of new materials, in particular mineral or mineral-like species. Oxalate minerals, which are formed when the metabolic products of bacteria, micromycetes and lichens interact with rocks and minerals [21,22,23,24], can be regarded as a striking example of such interactions. Oxalic acid is not the only known product of the living cycle; organic acids such as acetic, citric, formic, and etc. were also detected among the metabolites of microorganisms [23]. Thus, one could expect the crystallization of various organic acids salts. However, in nature, mainly oxalates are found in macroscopic amounts, which is due to their low solubility. Even though formic acid was found as a metabolite of a number of microorganisms [25], formation of biogenic formates, similar to oxalate mineralization, is unlikely, due to the higher solubility of its salts and the fast consumption of formate by bacterial consortiums. To date, there are no findings of formates formed as a result of interaction of microorganisms with rocks and minerals. In this regard, the processes occurring in Alkali Lake as a result of specific biogeochemistry features, associated, among other things, with the pollution of the lake, created unique conditions for inhibition of methanogenesis, which lead to exceptional biogenic crystallization of formic acid salts.

The unusual accumulation of formate as centimeter-sized calcium formate crystals is a remarkable phenomenon from the viewpoint of formate biogeochemistry. Formate is an important metabolic intermediate and electron carrier in syntropic bacterial consortiums of anaerobic acetogens and methanogens [26]. Formate is excreted as the end-product of fermentation of organic materials, mainly by the action of pyruvate-formate lyase during acetogenic and ethanolic fermentation in both prokaryotes and eukaryotic anaerobes [27,28,29,30]. In the sediments of haloalkaline lakes, the presence of acetogenic fermentative bacteria could lead to elevated formate and acetate, used by methylotrophic methanogens or rapidly consumed by aerobic heterotrophic bacteria. Considering that methanogenesis was possibly a predominant process in the anoxic sediments, we assumed that the formate/acetate generated by anaerobic fermentation of organic matter produced by photosynthetic and heterotrophic aerobes in the oxic zone, may be a source of one carbon unit for the metabolism of the consortium of methanogens and methanotrophs [31,32]. To confirm the biogenic origin of the formate in the Ca(HCO₂)₂ crystals collected at Alkali Lake, we measured the carbon isotope composition of calcium formate, and associated gaylussite and sodium carbonate in the sediments. The δ¹³C value observed in carbonates was −0.6‰, consistent with the equilibration with atmospheric CO₂ and weathering origin of carbonates [33], and with the values observed for dissolved inorganic carbon above the chemocline in soda lake waters [34]. Instead, the observed carbon isotope abundance in formate was δ¹³C = −26.5‰, consistent with the δ¹³C of organic carbon observed in soda lake sediments (about −20‰ [34]).

The strong accumulation of formate which lead to the crystallization of Ca(HCO₂)₂ can be explained either on the basis of the lake microbiology or as a consequence of anthropogenic pollution. The solution of this problem is relevant regarding the environmental consequences and transformation of pollutants. The methanogens isolated in the subsurface sediments of Alkali Lake belong mainly to the order Methanosarcinales, which are not able to grow using formate as a substrate; a methanogen community with a limited capacity for formate consumption could have favored its accumulation in the sediments [35,36]. This circumstance, together with the relative low solubility of calcium formate and desiccation of lake shores, could lead to the unique conditions of formate crystallization in Alkali Lake. On the other hand, in 1969 to 1971, the area near Alkali Lake was used as a waste storage area, and in 1976, production waste containing chlorophenolic compounds were released into the lake [37,38]. The released pollutants included 5000 cubic meters (25,000 200 L drums) of the 2,4-dichlorophenoxyacetic acid (2,4-D) manufacture byproducts, a tactic warfare defoliant used under the names “herbicide orange” and “Agent Orange” during the Vietnam war [39,40,41]. These compounds, as well as other organochlorines, are strong inhibitors of methanogenesis, leading to the accumulation of formate [26,42]. The significant entry of organic pollutants in the lake sediments could have contributed to the increase of anoxia and the production of formate by anaerobic fermentation, but we think that pollutants were not a significant primary carbon source for the formate; there were no direct metabolic routes to formate from these pollutants, and, furthermore, if the pollutants were the carbon source, we would expect a lower δ¹³C(formate), in the range from −30‰ to −40‰, consistent with the isotope abundances of synthetic pollutants [43]. Instead, the carbon isotope abundances were expected for biogenic organic matter in sediments of a soda lake. Hence, the inhibition of methanogenesis in the anoxic sediments, possibly induced by industrial pollutants, led to the increase of formate concentration. It is possible that this increase, together with the ease of formate salts to form macroscopic crystals and the calcium saturation of the lake water, led to the unique crystallization of Ca formate observed in Alkali Lake (Figure 5).

Orthorhombic α-Ca(HCO₂)₂ was easily obtained by slow crystallization from aqueous solutions [11]. Thus, this polymorph was most stable at normal conditions. This assumption was in agreement with the occurrence of this phase in the lacustrine sediments, as well as with the fact that α-Ca(HCO₂)₂ has the largest density (of 2.040 g/cm³) among the Ca formate polymorphs. It was of interest that formicaite, a β-modification of Ca(HCO₂)₂ with the density of 1.991 g/cm^3, was described in nature prior [1] to α-Ca(HCO₂)₂, which indicated that tetragonal β-calcium formate was also stable at ambient conditions, but there should be some stabilization mechanism for its occurrence. For instance, stabilization of low-density polymorphs by low amounts of enclathrated molecules is a usual phenomenon. Melanophlogite, a low-density cubic SiO₂ modification stabilized by enclathrated CH₄ and N₂ molecules [44], and low-density modifications of 2,4,6,8,10,12-hexanitro-2,4,6,8,10,12-hexaazaisowurtzitane stabilized by enclathrated H₂O and H₂O₂ molecules [45,46] can be given as an examples. Both formicaite discoveries (in both Novofrolovskoe and Solongo boron-rich skarn deposits) were confined to associations of boron minerals. Thus, one cannot exclude that trace amounts of any boron-bearing species may stabilize the low-density β-Ca(HCO₂)₂ structure.