DOCSLIB.ORG

Character and Distribution of Nonclastic Minerals in the Searles Lake Evaporite Deposit California

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text

Load more

Character and Distribution of Nonclastic Minerals in the Searles Lake Evaporite Deposit California By GEORGE I. SMITH and DAVID V. HAINES I CONTRIBUTIONS TO GENERAL GEOLOGY GEOLOGICAL SURVEY BULLETIN 1181-P Prepared in cooperation with the State of California, Resources Agency, ' Department of Conservation, Division of Mines and Geology -A UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1964 UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director The U.S. Geological Survey Library catalog card for this publication appears after page P58. For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402 CONTENTS Page Abstract..---.---------------------------------------------------- PI Introduction-____________-___-___----_--_-______-____--_______-___ 3 Acknowledgments ____-_____---_-__--__--_----__-_______---____..__- 4 Mineralogy __________-_---_---------_-_--_----_-------_--__-_-____ 6 , Minerals associated with saline layers____________________________ 8 Aphthitalite.. __-____---_----_---_--___---_---__-_________ 8 Borax-----.--------------------------------------.------- 10 Burkeite__.______--____-_.._-___-._-__.____..._..______ 12 Halite ------------------------------------------------- 14 Hanksite.-_------------_-----_-------__----------_----__- 16 Nahcolite__-___-_---_-_______-___-___---_____-___-_-____ 18 ^ Sulfohalite-.--------------------------------------------- 19 Teepleite._-----------------_----_------_-------_---_-.-.- 20 ,- Thenardite...-----__-_----__-------__------__.---.--__--- 20 Tincalconite______________________________________________ 21 < Trona---_--------_---------------_-------------------_. 21 Minerals associated with mud layers ----------------------------- 24 Adularia. ________________________________________________ 24 Analcime._ _______________________________________________ 25 Aragonite__._.--___-._-___--_-.---___-__.______-_______- 25 '. Calcite.-------------------------------------------------- 25 Dolomite...----_-----.-__-_--------__-----_------.-_----- 26 * Galeite---.-----__----.__--_-------_------._-----.-------_ 27 Gaylussite.---___-___-____--_-_-______--___-_____-___--__- 27 Mirabilite.----------------_----.---._----_-.-----_------- 30 Northupite._..-__._._._._...__-__._.____...-____..__-.-._ 30 ' Phillipsite--------.---.-__---_--._.-.---.-.---.-.-.------- 31 Pirssonite __ _____________________________________________ 31 Schairerite..______________________________________________ 32 ., Searlesite.._______________________________________________ 33 Tychite._.--..---.-_-...-...-..-..-_..--._-..._..-..-.--_ 33 '> Summary of mineral occurrences. _______________________________ 33 Overburden Mud__---------------------------------------- 34 ^ Upper Salt ------------_-----_----..--.---------..------ 34 Parting Mud--..-----.-._.-.--..---.---.-----_----------- 34 Lower Salt__-___--__--____________________._______________ 55 ^ Bottom Mud.__________________________________________ 36 Mixed Layer......________________________________________ 37 ~/ Significance of variation in physical character of minerals.-.-------- 38 Differences in crystal sizes._________________________________ 38 ".J Differences in development and preservation of crystal faces.._- 40 Differences in crystal habit. ________________________________ 40 Halite.._.---....-_...._--.__.._...__---_---.---..-.-- 41 Borax_----________-___--___.____..__________._.______ 42 Trona _____________________________________________ 42 ,__ Hanksite.-_--_.-.--._-_________-_.___.__._-___.___--- 43 in IV CONTENTS Page Lake history indicated by character and distribution of minerals----.--.- P44 Minerals in the saline layers. _____:_____________________________ 46 Mixed Layer.----.---------------------------------------- 47 Saline layers in Lower Salt--_____--_--_-______-__.______-___ 47 Upper Salt________-----__--_-__----__-----__--____-____ 50 Minerals in the mud layers- --._----__.--_____----____-_______-_ 51 Mixed Layer____-_--__-_------_------------------_----_--- 53 Bottom Mud___--_.___.______-____---_--__-__--__---_.__ 53 Mud layers in Lower Salt.--.------....-._---_-____________- 54 Parting Mud________-_-----___________---_-_--__--_-__-_ 54 Overburden Mud._________________________________________ 55 References cited.._________________________________________________ 55 ILLUSTEATIONS Page FIGURE 1. Index map showing location of Searles Lake, Calif_________ P3 2. Subsurface stratigraphic units in the Searles Lake deposit- _ __ _ 5 3. Location of drill cores cited-_____________________________ 9 4-14. Photographs of: > 4. Borax crystals showing habits most commonly noted in Searles Lake__--_-____-___-___------_--_----_.-_ 10 5. Elongated borax crystals.__________________________ 11 6. Beds of trona separated by a lens of borax.___-__--_._ 12 7. Thin section across the bed of trona and borax shown in figure 6_--._---_----------------------------- 13 8. Large halite crystals in a vug___-________--____.__-_ 15 ^ 9. Hanksite crystals found in Searles Lake showing vari­ ation in habits-.-.--.----_______________________ 16 * 10. Hanksite and borax crystals._______________________ 17 \ 11. "Fishtail" twinned nahcolite crystals. _-___._._______ 19 12. Two forms of tincalconite. _________________________ 22 13. Trona blades penetrating borax.____________________ 24 14. Thin beds of aragonite in the Parting Mud.__________ 26 15. Sketches of relations between gaylussite and laminated muds. 29 f^ 16. Phase diagrams of the system NaHC03-Na2 C03-Na2SO4- NaCl-H2Oat 20° and 14° --._.....-..-...--..__-.-. 48 CONTRIBUTIONS TO GENERAL GEOLOGY CHARACTER AND DISTRIBUTION OF NONCLASTIC MIN­ ERALS IN THE SEARLES LAKE EVAPORITE DEPOSIT, CALIFORNIA By GEORGE I. SMITH and DAVID V. HAINES ABSTRACT The Searles Lake evaporite deposit, California, near the southwest corner of the Basin and Range province, was formed by a succession of late Quaternary lakes that filled the basin and then either shrank to form saline lakes or desic­ cated. The deposit crops out at the surface as a bed of nearly pure halite that covers an area of about 12 square miles; beneath the surface it consists of inter- bedded salines and muds that lie nearly flat and cover an area of about 40 square miles. This paper summarizes the areal and stratigraphic distribution of the nonclastic minerals in the deposit, correlates their characteristic forms with the stratigraphic units from which they came, and deduces the depositional history responsible for this distribution. A total of 25 nonclastic mineral species occur in Searles Lake; 10 of these species were first found in a natural state in this deposit. In terms of anions, 9 of the 25 minerals contain sulfate ; 8, carbonate or bicarbonate ; 7, chloride ; 4, bor- ate; 3, fluoride ; 3, aluminosilicate; and 1, borosilicate. In terms of cations, 20 of the 25 minerals contain sodium; 6, calcium ; 3, magnesium ; and 4, potassium. The minerals containing calcium and magnesium are chiefly carbonates ; the minerals bearing sodium and potassium may contain any of the listed anions. Ten of the 25 minerals contain water or hydroxyl ions. The distributions and characteristic forms of these minerals are different in each of the stratigraphic units. The Overburden Mud (late Recent) consists predominantly of interbedded dark-brown mud and cubo-octahedral or water- rounded halite. The Upper Salt (early Recent) consists chiefly of thick beds of cubo-octahedral crystals of halite, pyramidal crystals of hanksite, megascopic to microscopic crystals of acicular trona, and thin beds of borax. The Parting Mud (late Wisconsin) consists of mud containing subhedral to anhedral crys­ tals of gaylussite and pirssonite, with subhedral to massive borax at the top, and local concentrations of microscopic crystals of dolomite, aragonite, halite, gaylus­ site, and pirssonite. In the Lower Salt (middle Wisconsin) each of the seven saline units and six mud units has a distinct mineral character. In the upper two saline units, intermixed aggregates of fine-grained and coarse-grained acicur lar trona predominate, but cubo-octahedral halite is locally abundant; the two thin mud layers underlying these units contain subhedral to anhedral mega­ scopic gaylussite, a smaller percentage of euhedral pirssonite, and microscopic PI P2 CONTRIBUTIONS TO GENERAL GEOLOGY crystals of both. The underlying two saline units consist chiefly of fine-grained trona, cubo-octahedral halite, and finely crystalline burkeite; the mud layers below them contain megascopic and microscopic crystals of gaylussite and nor- thupite and prismatic crystals of borax. The lowest three saline units are com­ posed chiefly of intermixed aggregates of fine-grained acicular trona and coarse­ grained bladed trona ; the two mud layers that separate them contain fine-grained aragonite and northupite and megascopic gaylussite. The Bottom Mud (early Wisconsin), which is about 100 feet thick, is composed chiefly of mud containing subhedral to anhedral gaylussite, but also contains small quantities of halite, thenardite, nahcolite, dolomite, calcite, tychite, pirssonite, northupite, borax, trona, mirabilite, analcime, adularia, and searlesite. The Mixed Layer (Illi- noian? and Sangamon?) is a series of interbedded muds and salines that has not been well explored. The layer consists chiefly of cubic halite, acicular trona, and muds, which here, as well as throughout the rest of the deposit, are composed of microscopic crystals of evaporites,
Recommended publications
  • How to Identify Rocks and Minerals

    How to Identify Rocks and Minerals

    How to Identify Rocks and Minerals fluorite calcite epidote quartz gypsum pyrite copper fluorite galena By Jan C. Rasmussen (Revised from a booklet by Susan Celestian) 2012 Donations for reproduction from: Freeport McMoRan Copper & Gold Foundation Friends of the Arizona Mining & Mineral Museum Wickenburg Gem & Mineral Society www.janrasmussen.com ii NUMERICAL LIST OF ROCKS & MINERALS IN KIT See final pages of book for color photographs of rocks and minerals. MINERALS: IGNEOUS ROCKS: 1 Talc 2 Gypsum 50 Apache Tear 3 Calcite 51 Basalt 4 Fluorite 52 Pumice 5 Apatite* 53 Perlite 6 Orthoclase (feldspar group) 54 Obsidian 7 Quartz 55 Tuff 8 Topaz* 56 Rhyolite 9 Corundum* 57 Granite 10 Diamond* 11 Chrysocolla (blue) 12 Azurite (dark blue) METAMORPHIC ROCKS: 13 Quartz, var. chalcedony 14 Chalcopyrite (brassy) 60 Quartzite* 15 Barite 61 Schist 16 Galena (metallic) 62 Marble 17 Hematite 63 Slate* 18 Garnet 64 Gneiss 19 Magnetite 65 Metaconglomerate* 20 Serpentine 66 Phyllite 21 Malachite (green) (20) (Serpentinite)* 22 Muscovite (mica group) 23 Bornite (peacock tarnish) 24 Halite (table salt) SEDIMENTARY ROCKS: 25 Cuprite 26 Limonite (Goethite) 70 Sandstone 27 Pyrite (brassy) 71 Limestone 28 Peridot 72 Travertine (onyx) 29 Gold* 73 Conglomerate 30 Copper (refined) 74 Breccia 31 Glauberite pseudomorph 75 Shale 32 Sulfur 76 Silicified Wood 33 Quartz, var. rose (Quartz, var. chert) 34 Quartz, var. amethyst 77 Coal 35 Hornblende* 78 Diatomite 36 Tourmaline* 37 Graphite* 38 Sphalerite* *= not generally in kits. Minerals numbered 39 Biotite* 8-10, 25, 29, 35-40 are listed for information 40 Dolomite* only. www.janrasmussen.com iii ALPHABETICAL LIST OF ROCKS & MINERALS IN KIT See final pages of book for color photographs of rocks and minerals.
  • Brine Evolution in Qaidam Basin, Northern Tibetan Plateau, and the Formation of Playas As Mars Analogue Site

    Brine Evolution in Qaidam Basin, Northern Tibetan Plateau, and the Formation of Playas As Mars Analogue Site

    45th Lunar and Planetary Science Conference (2014) 1228.pdf BRINE EVOLUTION IN QAIDAM BASIN, NORTHERN TIBETAN PLATEAU, AND THE FORMATION OF PLAYAS AS MARS ANALOGUE SITE. W. G. Kong1 M. P. Zheng1 and F. J. Kong1, 1 MLR Key Laboratory of Saline Lake Resources and Environments, Institute of Mineral Resources, CAGS, Beijing 100037, China. ([email protected]) Introduction: Terrestrial analogue studies have part of the basin (Kunteyi depression). The Pliocene is served much critical information for understanding the first major salt forming period for Qaidam Basin, Mars [1]. Playa sediments in Qaidam Basin have a and the salt bearing sediments formed at the southwest complete set of salt minerals, i.e. carbonates, sulfates, part are dominated by sulfates, and those formed at the and chlorides，which have been identified on Mars northwest part of basin are partially sulfates dominate [e.g. 2-4]. The geographical conditions and high eleva- and partially chlorides dominate. After Pliocene, the tion of these playas induces Mars-like environmental deposition center started to move towards southeast conditions, such as low precipitation, low relative hu- until reaching the east part of the basin at Pleistocene, midity, low temperature, large seasonal and diurnal T reaching the second major salt forming stage, and the variation, high UV radiation, etc. [5,6]. Thus the salt bearing sediments formed at this stage are mainly playas in the Qaidam Basin servers a good terrestrial chlorides dominate. The distinct change in salt mineral reference for studying the depositional and secondary assemblages among deposition centers indicates the processes of martian salts. migration and geochemical differentiation of brines From 2008, a set of analogue studies have been inside the basin.
  • Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States

    Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States

    BEST PRACTICES for: Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States First Edition Disclaimer This report was prepared as an account of work sponsored by an agency of the United States Government. Neither the United States Government nor any agency thereof, nor any of their employees, makes any warranty, express or implied, or assumes any legal liability or responsibility for the accuracy, completeness, or usefulness of any information, apparatus, product, or process disclosed, or represents that its use would not infringe privately owned rights. Reference therein to any specific commercial product, process, or service by trade name, trademark, manufacturer, or otherwise does not necessarily constitute or imply its endorsement, recommendation, or favoring by the United States Government or any agency thereof. The views and opinions of authors expressed therein do not necessarily state or reflect those of the United States Government or any agency thereof. Cover Photos—Credits for images shown on the cover are noted with the corresponding figures within this document. Geologic Storage Formation Classification: Understanding Its Importance and Impacts on CCS Opportunities in the United States September 2010 National Energy Technology Laboratory www.netl.doe.gov DOE/NETL-2010/1420 Table of Contents Table of Contents 5 Table of Contents Executive Summary ____________________________________________________________________________ 10 1.0 Introduction and Background
  • Mechanism. of Gypsification*

    Mechanism. of Gypsification*

    Geochimka. et Cofi!UOehimica Acta.1958, YoJ. 1&. py. 51 to 72. Pergamon :Press Ltd., London Mechanism. of gypsification* R. F. CoNLEYf and W. M. BUNDYt . (Recei11edl Aprill957; 1~71 rwi.sedform 24 Fehruary 1958) Abstract-Petrographic studies have shown that many gypsum deposits ha\>e been for111ed by the hydra-tion of anhydrit.,, but the mechanism for hydration has n~t been fully explained. Gypsum has been produced ~perimentally by the agitation of anhydrite in pure water, ~reaction that is accelerated by certa.in acids, bases, and salts, particularly aJkali sulphates. · Phase investigations and reaction velocity studies indicate that accelerated bydration of anhydrite takes place through the medium of transient surface wmplexes in cb1ute solution. Concentrated solutions may pre.cipita:te double salts. Contraa:y to recent hypotheses of gypsum dehydration by concentrated aalt solutions, double salt::; aniJfor gypsum are stable phases below a temuerature of 42°0. Abov6' 42"0 double salts may replace anhydrite as the stable pha..:.e. Gyps1.1.m. how~ver, may remain a roeta.stable phase indefinitely in its saturated solution below the hemih)'dmte transition temperature (98°C}. E;s:perimental data. indicate t.hat precipitation of anhydrite from sea. wat-er i.<J unlikely. INTRODUCTION HYDRATION of the mineral anhydrite (CaS011) to gypsum {CaS0 4 ·2~20) has been a well-known phenomenon for many years. Although the hydration of anhydrite by pure water is extremely slow, it is accelerated in the presence of certain salts, alkalis and acids. The mechanism whereby this acceleration takes place has never been fully understood.
  • Mineral Processing

    Mineral Processing

    Mineral Processing Foundations of theory and practice of minerallurgy 1st English edition JAN DRZYMALA, C. Eng., Ph.D., D.Sc. Member of the Polish Mineral Processing Society Wroclaw University of Technology 2007 Translation: J. Drzymala, A. Swatek Reviewer: A. Luszczkiewicz Published as supplied by the author ©Copyright by Jan Drzymala, Wroclaw 2007 Computer typesetting: Danuta Szyszka Cover design: Danuta Szyszka Cover photo: Sebastian Bożek Oficyna Wydawnicza Politechniki Wrocławskiej Wybrzeze Wyspianskiego 27 50-370 Wroclaw Any part of this publication can be used in any form by any means provided that the usage is acknowledged by the citation: Drzymala, J., Mineral Processing, Foundations of theory and practice of minerallurgy, Oficyna Wydawnicza PWr., 2007, www.ig.pwr.wroc.pl/minproc ISBN 978-83-7493-362-9 Contents Introduction ....................................................................................................................9 Part I Introduction to mineral processing .....................................................................13 1. From the Big Bang to mineral processing................................................................14 1.1. The formation of matter ...................................................................................14 1.2. Elementary particles.........................................................................................16 1.3. Molecules .........................................................................................................18 1.4. Solids................................................................................................................19
  • Mirabilite Na2so4 • 10H2O C 2001-2005 Mineral Data Publishing, Version 1

    Mirabilite Na2so4 • 10H2O C 2001-2005 Mineral Data Publishing, Version 1

    Mirabilite Na2SO4 • 10H2O c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Monoclinic. Point Group: 2/m. Crystals short to long prismatic, with complex form development, also crude, to 10 cm, in interlocking masses; crystalline, granular to compact massive, commonly as efflorescences. Twinning: Rare on {001} or {100}. Physical Properties: Cleavage: On {100}, perfect; on {010} and {001}, good to fair. Fracture: Conchoidal. Hardness = 1.5–2.5 D(meas.) = 1.464 D(calc.) = 1.467 Quickly dehydrates to th´enarditein dry air; very soluble in H2O, taste cool, then saline and bitter. Optical Properties: Transparent to opaque. Color: Colorless to white; colorless in transmitted light. Streak: White. Luster: Vitreous. Optical Class: Biaxial (–). Orientation: X = b; Z ∧ c =31◦. Dispersion: r< v,strong, crossed. α = 1.391–1.394 β = 1.394–1.396 γ = 1.396–1.398 2V(meas.) = 75◦560 Cell Data: Space Group: P 21/c (synthetic). a = 11.512(3) b = 10.370(3) c = 12.847(2) β = 107.789(10)◦ Z=4 X-ray Powder Pattern: Synthetic. (ICDD 11-647). 5.49 (100), 3.21 (75), 3.26 (60), 3.11 (60), 4.77 (45), 3.83 (40), 2.516 (35) Chemistry: (1) (2) SO3 25.16 24.85 Na2O 18.67 19.24 H2O 55.28 55.91 Total 99.11 100.00 • (1) Kirkby Thore, Westmoreland, England. (2) Na2SO4 10H2O. Occurrence: Typically in salt pans, playas, and saline lakes, where deposition may be seasonal, and bedded deposits formed therefrom; rarely in caves and lava tubes; in volcanic fumaroles; a product of hydrothermal sericitic alteration; a post-mining precipitate.
  • When “Evaporites” Are Not Formed by Evaporation: the Role Of

    When “Evaporites” Are Not Formed by Evaporation: the Role Of

    When “evaporites” are not formed by evaporation: The role of temperature and pCO2 on saline deposits of the Eocene Green River Formation, Colorado, USA Robert V. Demicco† and Tim K. Lowenstein Department of Geological Sciences and Environmental Studies, Binghamton University, Binghamton, New York 13902-6000, USA ABSTRACT INTRODUCTION rated with halite. During summer, the waters of the lake above the thermocline (at <25 m depth) Halite precipitates in the Dead Sea during Geologists studying salt deposits have noticed warm to ∼34 °C, become undersaturated with ha- winter but re-dissolves above the thermo- that very soluble minerals that occur in the cen- lite due to the temperature increase, and the bulk cline upon summer warming, “focusing” ha- ter of a basin do not extend out to the edges of of the winter-deposited halite above the thermo- lite deposition below the thermocline (Sirota the basin (Hsü et al., 1973; Dyni, 1981; Lowen- cline re-dissolves. Summer dissolution of halite et al., 2016, 2017, 2018). Here we develop an stein, 1988). This is true even where: (1) soluble occurs in the Dead Sea despite any increase in “evaporite focusing” model for evaporites salts are interpreted to have been deposited in evaporative concentration at the surface. The ha- (nahcolite + halite) preserved in a restricted a deep evaporitic lake or marine basin and (2) lite that settled into the deeper, cooler isothermal area of the Eocene Green River Formation deep-water deposits that encase salts in the cen- bottom waters, however, accumulates as an an- in the Piceance Creek Basin of Colorado, ter of the basin can be confidently traced to pe- nual layer at depths below the 25 m deep ther- USA.
  • Non-Clastic Sedimentary Rocks by Cindy Grigg

    Non-Clastic Sedimentary Rocks by Cindy Grigg

    Non-Clastic Sedimentary Rocks By Cindy Grigg 1 Rocks can be put into three main groups. They are grouped by how the rocks formed. Sedimentary (sed-uh-MEN-tuh-ree) rocks are formed on or near Earth's surface. Sedimentary rocks are sorted into other groups. They can be sorted as clastic or non-clastic. This group tells something about the rocks' beginning and what they formed from. 2 Non-clastic rocks are created when water evaporates or from the remains of plants and animals. Limestone is a non-clastic sedimentary rock. Limestone is made of the mineral calcite. It often contains fossils. Limestone formed in the ocean from the shells and skeletons of dead sea creatures. Some of the fossils in limestone are too small to be seen without a microscope. Chalk is a type of limestone that is usually white. It consists almost entirely of the shells of tiny dead sea creatures. Limestone is a common building material. 3 Coal is another non-clastic rock. It formed from the dead remains of plants. Millions of years ago, plants fell into swamps. They were covered with layers of sediment and did not rot. Over millions of years, as the remains were buried deeper under more and more layers of sediment, they were changed by pressure into coal. Coal is commonly used as fuel in power plants to make electricity. 4 Evaporite rocks formed when minerals such as gypsum and halite (rock salt) were left behind as water evaporated from oceans and lakes. Evaporite is common in desert areas, where evaporation is high, such as the Great Salt Lake in Utah.
  • Salt Crystallization in Porous Construction Materials I Estimation of Crystallization Pressure

    Salt Crystallization in Porous Construction Materials I Estimation of Crystallization Pressure

    View metadata, citation and similar papers at core.ac.uk brought to you by CORE provided by EPrints Complutense Salt crystallization in porous construction materials I Estimation of crystallization pressure A. La Iglesiaa,*, V. Gonzalezb, V. L6pez-Acevedoc, C. Viedmac , Inslituto de Geologia Economica del CSIC, Facultad de Ciencias Ge% gicas, UCM, E·280411 Madrid. Spain b Deparlamento de Quimica, ETSI, Agronomos, UPM, E·28IJ40 Madrid, Spain , Deparlamenlo de Cristalografia y Mineralogia, Facultad de Ciencias Ge% gicas, UCM. E·28040 Madrid, Spain Abstract The crystallization process of soluble salts inside the natural and artificial porous materials partially immersed in different saline solutions has been studied, This procedure is used to simulate the conditions of exposure to salt weathering in which foundations and lower walls of building structures are within the zone of capillary rise of saline ground water. Crystallization pressures that can develop in the samples, which are a function of the pore size and salt-solution interfacial tension, have been calculated and are compared with experimental values of the materials tensile strength. since both these parameters allow the prediction of porous materials behaviour against salt weathering. Keywords: Salt weathering; Porous media; Salt crystallization; Crystallization pressure 1. Introduction The problem of crystallization pressure of salt was first studied by Correns [6J, who presented The crystallization process of soluble salts in a workable equation based on the Riecke principle porous materials can generate pressures inside the from which the pressure generated P versus salt pores sufficient to exceed the elastic limit of the supersaturation may be calculated: material, causing its breakage.
  • The American Journal of Science

    The American Journal of Science

    THE AMERICAN JOURNAL OF SOIENOE. EDITOR: EDWARD S. DANA. ASSOCIATE EDITORS PROFESSORS GEO. L. GOODALE, JOHN TROWBRIDGE, H. P. BOWDITCH AND W. G. FARLOW, OF CAMBRIDGE, PROFESSORS O. C. MAHSH, A. E. VERRILL AND H. S. WILLIAMS, OF NEW HAVEN, PROFESSOR GEORGE F. BARKER, OF PHILADELPHIA, PROFESSOR H. A. ROWLAND, OF BALTIMORE, MR. J. S. DILLER, OF W ASHl~GTON. FOURTH SERIES. VOL. II-[WHOLE NUMBER, CLI!.] Nos. 7-12. JULY TO DEOEMBER, 1896. WITH SIX PLATES. NEW HAVEN, CONNECTICUT. 1896'. J. B. Pratt-Northupite, PirBsonite, etc. 123 , ART. ~V.-On Northupite; Pirs8onite, a new mineral j (}OI!flussite and IIanksite from Borax Lake, San Bernar­ dino County, Californi(t j by J. H. PRATT. INTRODUCTION. THE minerals to be described in this paper are from the remarkable locality of Borax Lake, San Bernardino County, California. They were broug-ht to the author's notice, in the fall of 1895, by Mr. Warren M. Foote of Philadelphia, who sent one of them, the northupite, tog-ether with some of the associ­ ated minerals, to the mineralogical laboratory of the Sheffield Scientific School, for chemical investigation. About the same time Mr. C. H. Northup of San Jose, CaL, sent some minerals from the same region to Prof. S. L. Penfield. Among them, gaylussite, hanksite and a third mineral, which has proved to be a new species, were identified. These same minerals were also observed among the specimens sent by Mr. Foote. Mr. Northup, in his letter of transmittal, stated that he had care­ fully saved all of the crystals of the new mineral, having observed that they were different from gaylnssite in habit, and that he believed they would prove to be a new and interesting species.
  • Gaylussite Na2ca(CO3)2 • 5H2O C 2001-2005 Mineral Data Publishing, Version 1

    Gaylussite Na2ca(CO3)2 • 5H2O C 2001-2005 Mineral Data Publishing, Version 1

    Gaylussite Na2Ca(CO3)2 • 5H2O c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Monoclinic. Point Group: 2/m. As flattened wedge-shaped crystals with dominant {110}, {011}, {001}, smaller {010}, {100}, {101}, {112}; also as prismatic to dipyramidal crystals elongated along [100], to 6 cm. Physical Properties: Cleavage: On {110}, perfect; on {001}, imperfect. Fracture: Conchoidal. Tenacity: Very brittle. Hardness = 2.5–3 D(meas.) = 1.991 D(calc.) = 1.991 Dehydrates with efflorescence in dry air; slowly decomposes in H2O leaving CaCO3 as calcite or aragonite. Optical Properties: Transparent to translucent. Color: Colorless to pale yellow or pale gray, white; colorless in transmitted light. Streak: White to pale gray. Luster: Vitreous. Optical Class: Biaxial (–). Orientation: X = b; Z ∧ c = –15◦. Dispersion: r< v,strong, crossed. α = 1.444 β = 1.516 γ = 1.523 2V(meas.) = 34◦ Cell Data: Space Group: C2/c. a = 11.589 b = 7.780 c = 11.207 β = 102.5◦ Z=4 X-ray Powder Pattern: John Hay, Jr. Well No. 1, Wyoming, USA. 6.403 (100), 3.18 (80), 2.70 (80), 2.61 (80), 1.91 (80), 2.49 (70), 1.98 (70) Chemistry: (1) (2) CO2 30.02 29.72 SiO2 0.08 Fe2O3 0.03 MnO 0.01 MgO 0.01 CaO 19.02 18.94 Na2O 20.40 20.93 H2O 30.47 30.41 insol. 0.16 Total 100.20 100.00 • (1) Taboos-nor salt lake, Mongolia. (2) Na2Ca(CO3)2 5H2O. Occurrence: Typically in evaporites or shales from alkali lakes; rarely in veinlets cutting alkalic igneous rocks.
  • National Evaporite Karst--Some Western Examples

    National Evaporite Karst--Some Western Examples

    122 National Evaporite Karst--Some Western Examples By Jack B. Epstein U.S. Geological Survey, National Center, MS 926A, Reston, VA 20192 ABSTRACT Evaporite deposits, such as gypsum, anhydrite, and rock salt, underlie about one-third of the United States, but are not necessarily exposed at the surface. In the humid eastern United States, evaporites exposed at the surface are rapidly removed by solution. However, in the semi-arid and arid western part of the United States, karstic features, including sinkholes, springs, joint enlargement, intrastratal collapse breccia, breccia pipes, and caves, locally are abundant in evaporites. Gypsum and anhydrite are much more soluble than carbonate rocks, especially where they are associated with dolomite undergoing dedolomitization, a process which results in ground water that is continuously undersaturated with respect to gypsum. Dissolution of the host evaporites cause collapse in overlying non-soluble rocks, including intrastratal collapse breccia, breccia pipes, and sinkholes. The differences between karst in carbonate and evaporite rocks in the humid eastern United States and the semi-arid to arid western United States are delimited approximately by a zone of mean annual precipitation of 32 inches. Each of these two rock groups behaves differently in the humid eastern United States and the semi-arid to arid west. Low ground-water tables and decreased ground water circulation in the west retards carbonate dissolution and development of karst. In contrast, dissolution of sulphate rocks is more active under semi-arid to arid conditions. The generally thicker soils in humid cli- mates provide the carbonic acid necessary for carbonate dissolution. Gypsum and anhydrite, in contrast, are soluble in pure water lacking organic acids.