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Larimar – a unique pectolite rock from the Dominican Republic

Kowalczyk J., Natkaniec-Nowak L., Wachowiak J.

Geology, Geophysics and Environment

2015

Vol. 41, no. 1

101--102

Larimar, whose colour is varying from white light-blue, green-blue to deep blue, is only found in the Sierra de Bohoruco mountain range, Barahona Province, the Dominican Republic. It was discovered by a Spanish priest, Miguel Fuertes Lorén, in 1916 (Fuertes Marcuello & Garcia Guinea 1990). On the basis of geological map of this region, larimar is found in a tectonic sheet of Cretaceous-Eocene rocks, mainly basalts, tuffs and tuffites which are associated to an emerged block of oceanic Caribbean crust. The basic host rock is highly serpentinized and has suffered intensive fracturing and shearing (Donnelly et al. 1990). The Dumisseau formation represented by volcanic rocks is over-lain by limestones of the “Neiba formation” of the Lower Eocene-Lower Miocene age. During most of the Eocene, these carbonate rocks coexisted with, or were replaced by, volcanic materials of a tholeitic to alkaline signature (OIT to OIA), grouped under the new denomination of El Aguacate de Neiba Volcano-Sedimentary Complex, interpreted as being associated with plume. In the northern and southern areas of the Sierra de Bohoruco, coral reef limestones were deposited, representing shallow platform environments of the Oligocene-Miocene age (Huerta et al. 2007). Fault contacts are observed between the volcanic and the limestone rocks (Bente et al. 1991). For the first time, larimar was defined as a pectolite rock by the authors of this paper. The reason for this definition is the rock’s macroscopic, heterogeneous character emphasized by finely fibrous, spheroidal aggregates. The heterogeneity is also observed in the mineral composition of the rock. Pectolite, as a major component in these rocks, is a triclinic mineral crystallized usually in veinlets, stringers, and irregular masses in volcanic rocks. Other minerals, such as calcite, natrolite, chalcedony, hematite, chalcocite, crystal formations, and occasionally hematite dendrites, coexist with pectolite and are located along the border fillings (Woodruff & Fritsch 1989). Apatite, sphene, prehnite, danburite and datolite were also found in these heterogeneous masses (Fuertes Marcuello & Garcia Guinea 1990). In addition, Espi & Borrego described in 2008 an organic material associated with pectolite (indentified as volatiles), as a material which was very similar in appearance to bituminouscoal. Due to the heterogeneous character and various mineral compositions, the rock’s colour changes within short distances, and shows other colours-nearly white to light greenish, greenish to greenish blue, and light bluish to blue. The origin of the larimar colour is still not obvious. It has been associated with the presence of copper coming from copper sulphide (Woodruff & Fritsch 1989). Bente et al. (1991) suggested that vanadium was the cause of the colouration and the authors did not exclude the presence of other possible elements like Fe, Ti, Cr, Co, or Ni. Using a thermoluminescence dating, in light blue and blue pectolite were confirmed trace amounts of manganese (Sullasi et al. 2010). Woodruff & Fritsch (1989) are not excluded a manganese as a colouring agent. Espi & Borrego suggested in 2008 that organic matter might have been related to the larimar coloration. The petrographic studies of pectolite samples by Espi & Borrego (2008) with SEM-EDS showed that the veins containing pectolite were associated with a variety of minerals like apatite, calcite, and impure hematite, which, except for iron and oxygen, consisted of aluminium, titanium, calcium, and gold. The chemical composition of the veins, with almost an isometric crystal and compound Mg, Al, Si, Fe, K and Au, suggested the pyroxene group. SEM-EDS analyses of two samples of that rock conducted by the authors showed that impure hematite spreading in that crystalline groundmass can give alike results in polymineral composition, as colour-bearing elements, like Cr and Cu. Small amounts of copper are also found together with the pectolites. Some magnesium ions occurring within pectolite aggregates suggest that this element replaced calcium ions in the pectolite structure. Its source may be found in the surrounding original wall rock, especially in pyroxene group, represented by augite. That latter group is also represented by diopside, which is typical for serpentinization as the replacement of the wall rock. Association of pectolite with a variety of minerals, including e.g. hematite, calcite, natrolite, chalcedony, apatite, chalcocite, and crystallizations in veinlets, stringers, and irregular masses in volcanic rocks suggestes hydrothermal genesis of pectolite. The temperature in which it was formed did not exceed 250°C (Bente et al. 1991) and the process was strongly associated with reduced CO2 concentrations in solutions and low pressure zones (Włodyka et al. 1999).The above conditions were found to occur in many places around the world. The question is why the bluish pectolite crystallized only in one country, the Dominican Republic.

Nowe elementy w tektonice płaszczowiny kriżniańskiej między Doliną Bystrej a Doliną Strążyską w Tatrach

Zabielski R., Iwanow A.

Przegląd Geologiczny

2014

Vol. 62, nr 2

86--96

The Sub-Tatric units was newly mapped for the implementation of the Detailed Geological Map of the Tatra Mountains at the scale of 1 : 10 000 (SmgT). Lithostratigraphic andtectonic field observations between the Bystra Valley and the Strążyska Valley allowed a newinterpretation of the geological structure of the area. The system of sheets has appeared to beeven more complicated than that advocated by Guzik and Kotański (1963). New sheets have been recognized: Grześkówki sheets (Lower and Upper sheets), which were distinguished from the former Grześkówki sheet (sensu Guzik & Kotański, 1963), and the Kazalnica sheet and Żywczańskie sheet, which were distinguished from the Samkowa Czuba sheet. Both Grześkówki sheets and Kazalnica sheet are composed of Carnian and Norian clastics or marly dolomites, Rhaetian limestones and Hettangian clayey-silty shales. The Lower Grzeoekówki and Kazalnica sheets lie in the inverted position and Żywczańskie sheet is composed of an isolated package of Lower Jurassic spotted marls and limestones lying in the normal position contrary to the inverted beds of the Samkowa Czuba sheet. The Spadowiec sheet has a wider spatial extent than it was postulated earlier. The Jastrzębia Turnia sheet probably does not exist in area between the valleys of Białego and Bystra.