Volcanic Rocks of the Cienega Area, Santa Fe County, New Mexico

Total Page:16

File Type:pdf, Size:1020Kb

Volcanic Rocks of the Cienega Area, Santa Fe County, New Mexico BULLETIN 54 Volcanic Rocks of the Cienega Area, Santa Fe County, New Mexico by MING-SHAN SUN and BREWSTER BALDWIN Sequence and geochemistry of Cenozoic volcanic rock units, with a discussion of the norm classification 1 9 5 8 STATE BUREAU OF MINES AND MINERAL RESOURCES NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY CAMPUS STATION SOCORRO, NEW MEXICO NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY E. J. Workman, President STATE BUREAU OF MINES AND MINERAL RESOURCES Alvin J. Thompson, Director THE REGENTS MEMBERS Ex OFFICIO The Honorable Edwin L. Mechem .................. Governor of New Mexico Mrs. Georgia L. Lusk ........................ Superintendent of Public Instruction APPOINTED MEMBERS Robert W. Botts ................................................................. Albuquerque Holm 0. Bursum, Jr. .................................................................. Socorro Thomas M. Cramer .................................................................. Carlsbad John N. Mathews, Jr. ................................................................. Socorro Richard A. Matuszeski ....................................................... Albuquerque Contents Page ABSTRACT ...................................................................................................... 1 INTRODUCTION ......................................................................................... 3 Purpose .......................................................................................................... 3 Setting ............................................................................................................ 3 Previous work ............................................................................................... 5 Method of work ........................................................................................... 5 Acknowledgments ....................................................................................... 6 FIELD RELATIONSHIPS (by Brewster Baldwin) ................................... 7 Stratigraphy ................................................................................................... 7 Cretaceous mudstone ............................................................................... 8 Galisteo formation .................................................................................... 8 Andesite breccia ...................................................................................... 10 Augite monzonite ................................................................................... 11 Calcic latite .................................................................................................. 12 Glassy latite .............................................................................................. 13 Units of uncertain stratigraphic position ............................................. 14 Volcanic conglomerate ...................................................................... 14 Augite basalt ........................................................................................ 14 Hornblende andesite dike ................................................................. 14 Vent breccia ......................................................................................... 15 Felsite dike ........................................................................................... 15 Cieneguilla limburgite ............................................................................. 15 Ancha formation ..................................................................................... 18 Basalt ......................................................................................................... 18 Terrace gravel ............................................................................................. 19 Alluvium ...................................................................................................... 19 Cover ............................................................................................................ 19 Age and correlation ................................................................................... 19 Structure ......................................................................................................... 23 LABORATORY STUDIES (by Ming-Shan Sun) .................................... 26 Petrography ................................................................................................. 26 Introduction ............................................................................................. 26 The term "monzonite" ........................................................................... 26 Andesite breccia ...................................................................................... 27 iii Page Augite monzonite ................................................................................... 29 Calcic latite ............................................................................................... 30 Hornblende andesite .............................................................................. 31 Glassy latite .............................................................................................. 31 Felsite ....................................................................................................... 32 Vent breccia ............................................................................................. 33 Cieneguilla limburgite ............................................................................ 33 Olivine basalt ........................................................................................ 34 Limburgite ............................................................................................ 34 Basalt ........................................................................................................ 35 Petrology ...................................................................................................... 36 Norm classification ..................................................................................... 38 Weight norm ........................................................................................... 40 Molecular norm........................................................................................ 41 Norms of the Cienega rocks ................................................................. 45 Geochemical aspects .................................................................................. 45 Index of refraction ................................................................................. 45 General discussion .............................................................................. 45 Artificial glasses .................................................................................... 48 Chemical composition ........................................................................... 51 Minor constituents .............................................................................. 51 Major constituents ............................................................................... 54 APPENDIX I .................................................................................................. 59 Rules for the calculation of norms ............................................................ 59 Weight norm ........................................................................................... 60 Molecular norm ...................................................................................... 64 APPENDIX II ................................................................................................ 69 Summary of data from rock samples, Cienega area, New Mexico 69 REFERENCES ............................................................................................... 74 INDEX ............................................................................................................. 77 Illustrations TABLES 1. Rock units of the Cienega area, New Mexico ....................................... 7 2. Orthoclase-plagioclase ratios of the Cienega monzonite, latite, and andesite, in comparison with those of Daly's average monzonite, andesite, and diorite .......................................................... 27 iv Page 3. Grain-size analysis of disintegrated andesite breccia .................... 28 4. The C.I.P.W. weight norms of seven volcanic rocks, Cienega area, New Mexico .................................................................................. 43 5. The molecular norms of seven volcanic rocks, Cienega area, New Mexico ........................................................................................... 44 6. Effect of various oxides on the index of refraction of glasses of binary or ternary system with silica ..................................................... 46 7. The ionic density of the cations which occur as modifiers in silicate glass ............................................................................................. 47 8. Lower limits of spectrographic detection ....................................... 51 9. Minor constituents of the Cienega volcanic rocks ........................ 53 10. Chemical composition of seven volcanic rocks, Cienega area, New Mexico ........................................................................................... 54 11. Modified Holmquist formulae .......................................................... 55 12. Calculation of standard rock cell of olivine basalt of the Cienega area ...........................................................................................
Recommended publications
  • Geologic Map of the Simcoe Mountains Volcanic Field, Main Central Segment, Yakama Nation, Washington by Wes Hildreth and Judy Fierstein
    Prepared in Cooperation with the Water Resources Program of the Yakama Nation Geologic Map of the Simcoe Mountains Volcanic Field, Main Central Segment, Yakama Nation, Washington By Wes Hildreth and Judy Fierstein Pamphlet to accompany Scientific Investigations Map 3315 Photograph showing Mount Adams andesitic stratovolcano and Signal Peak mafic shield volcano viewed westward from near Mill Creek Guard Station. Low-relief rocky meadows and modest forested ridges marked by scattered cinder cones and shields are common landforms in Simcoe Mountains volcanic field. Mount Adams (elevation: 12,276 ft; 3,742 m) is centered 50 km west and 2.8 km higher than foreground meadow (elevation: 2,950 ft.; 900 m); its eruptions began ~520 ka, its upper cone was built in late Pleistocene, and several eruptions have taken place in the Holocene. Signal Peak (elevation: 5,100 ft; 1,555 m), 20 km west of camera, is one of largest and highest eruptive centers in Simcoe Mountains volcanic field; short-lived shield, built around 3.7 Ma, is seven times older than Mount Adams. 2015 U.S. Department of the Interior U.S. Geological Survey Contents Introductory Overview for Non-Geologists ...............................................................................................1 Introduction.....................................................................................................................................................2 Physiography, Environment, Boundary Surveys, and Access ......................................................6 Previous Geologic
    [Show full text]
  • The Oxidation Ratio of Iron in Coexisting Biotite And
    1423 The Canadian Mineralo gist Vol.37. pp. 1423-1429(1999\ THE OXIDATIONRATIO OF IRON IN COEXISTINGBIOTITE AND HORNBLENDEFROM GRANITICAND METAMORPHICROCKS: THE ROLE OF P, T AND f(O2) NADINES. BORODINA, GERMAN B. FERSHTATER$erro SERGEI L. VOTYAKOV Institute of Geology and Geochemistry, RussianAcademy of Sciences,Pochtoty per., 7, Eknterinburg, 620151, Russia Assrnecr Previously published and new data on the composition of coexisting biotite and homblende from granitic and metamorphic rocks show that the degree of iron oxidation, R [= Fe3*/(Fe2*+ Fe3*)], is different in these two minerals; the R of hornblende is greater. Granulite-facies minerals have the greatest difference in R, whereas in granitic rocks, those minerals show the least difference The oxidation of biotite and hornblende under high-level conditions is accompaniedby the crystallization of magnet- ite, and newly formed oxidized mafic minerals have a lower Fe/(Fe + Mg) and R than the original ones. Under mesozonal and catazonalconditions, the increasein pressureprevents the formation of magnetite, and oxidation is accompaniedby a significant increase in R; these changes in the chemical composition of hornblende are supplementedby an increase in Al. Since the Al content of homblende is known to be an indicator of pressure, such a correlation of R and Fer+ content with aluminum content points to an increaseof theseparameters with a rise of pressure Keywords:biotite, hornblende,oxidation ratio, granitic rocks, metamorphic rocks, epizonal plutons, mesozonalplutons , cat^7'onal plutons. Sorravarnr, Les donn6esnouvelles et celles tirde de la litt6rature portant sur 1acomposition de la biotite et celle de la hornblendecoexistante des roches granitiques et m6tamorphiquesmontrent qui le degrd d'oxydation du fer, R [= Fe3*/(Fe2*+ Fe3+)],est diffdrent dans ces deux mindraux.
    [Show full text]
  • The Geological Newsletter
    JAN 90 THE GEOLOGICAL NEWSLETTER ·• GEOLOGICAL SOCIETY OF THE OREGON COUNTRY GEOLOGICAL SOCIETY Non-Profit Org. U.S. POSTAGE OF THE OREGON COUNTRY PAID P.O. BOX ?a 7- Portland, Oregon PORTLAND, OR 97207- -:· ·--~··, Permit No. 999 - -- '~ Dr. Frank Boersma 120 W. 33~d Street Vancouver, WA 98660 GEOLOGICAL SOCIETY OF THE OREGOt\ COllNTRY 1989-1990 ADMINISTRATION BOARD OF DIRECTORS President Directors Rosemary Kenney 221-0757 Peter E. Baer (3 years) 661-7995 4211 S\-1 Condor Charlene Holzwarth (2 years) 284-3444 Portland, OR 97201 Esther Kennedy (1 year) 287-3091 Vice President Margaret L. Steere 246-1670 Immediate Past Presidents Joline Robustelli 223-2852 6929 SW 34 Ave. ~ Portland, OR 97219 R.E. (Andy) Corcoran 244-5605 Secretary Alta B. Fosback 641-6323 THE GEOLOGICAL NEWSLETTER 8942 SW Fairview Place Tigard, OR 97223 Editor: Sandra Anderson 775-5538 Treasurer Calendar: Margaret Steere 246-1670 Braden Pillow 659-6318 Business Manager: Carol Cole 220-0078 19562 SE Cottonwood St. Assist: Cecelia Crater 235-5158 Milwaukie, OR 97267 ACTIVITIES CHAIRS Calligrapher Properties and PA System Wallace R.· McClung 637-3834 (Luncheon) Donald Botteron 245-6251 Field Trips (Evening) Walter A. Sunderland 625-6840 Charlene Holzwarth 284-3444 Publications Alta B. Fosback 641-6323 Geneva E. Reddekopp 654-9818 Geology Seminars Publicity Donald D. Barr 246-2785 Roberta L. Walter 235-3579 Historian Refreshments Phyllis G. Bonebrake 289-8597 (Friday Evening) Hospitality David and Marvel Gillespie 246-2368 254-0135 (Luncheon) Margaret Fink 289-0188 Harold and Patricia Gay Moore (Evening) Maxine Harrington 297-ll86 (Geology Seminars) Catherine Evenson 654-2636 Library: Esther Kennedy 287-3091 ' ' Betty Turner 246-3192 Telephone n Past Presidents Panel Jean L.
    [Show full text]
  • (2000), Voluminous Lava-Like Precursor to a Major Ash-Flow
    Journal of Volcanology and Geothermal Research 98 (2000) 153–171 www.elsevier.nl/locate/jvolgeores Voluminous lava-like precursor to a major ash-flow tuff: low-column pyroclastic eruption of the Pagosa Peak Dacite, San Juan volcanic field, Colorado O. Bachmanna,*, M.A. Dungana, P.W. Lipmanb aSection des Sciences de la Terre de l’Universite´ de Gene`ve, 13, Rue des Maraıˆchers, 1211 Geneva 4, Switzerland bUS Geological Survey, 345 Middlefield Rd, Menlo Park, CA, USA Received 26 May 1999; received in revised form 8 November 1999; accepted 8 November 1999 Abstract The Pagosa Peak Dacite is an unusual pyroclastic deposit that immediately predated eruption of the enormous Fish Canyon Tuff (ϳ5000 km3) from the La Garita caldera at 28 Ma. The Pagosa Peak Dacite is thick (to 1 km), voluminous (Ͼ200 km3), and has a high aspect ratio (1:50) similar to those of silicic lava flows. It contains a high proportion (40–60%) of juvenile clasts (to 3–4 m) emplaced as viscous magma that was less vesiculated than typical pumice. Accidental lithic fragments are absent above the basal 5–10% of the unit. Thick densely welded proximal deposits flowed rheomorphically due to gravitational spreading, despite the very high viscosity of the crystal-rich magma, resulting in a macroscopic appearance similar to flow- layered silicic lava. Although it is a separate depositional unit, the Pagosa Peak Dacite is indistinguishable from the overlying Fish Canyon Tuff in bulk-rock chemistry, phenocryst compositions, and 40Ar/39Ar age. The unusual characteristics of this deposit are interpreted as consequences of eruption by low-column pyroclastic fountaining and lateral transport as dense, poorly inflated pyroclastic flows.
    [Show full text]
  • Source to Surface Model of Monogenetic Volcanism: a Critical Review
    Downloaded from http://sp.lyellcollection.org/ by guest on September 28, 2021 Source to surface model of monogenetic volcanism: a critical review I. E. M. SMITH1 &K.NE´ METH2* 1School of Environment, University of Auckland, Auckland, New Zealand 2Volcanic Risk Solutions, Massey University, Palmerston North 4442, New Zealand *Correspondence: [email protected] Abstract: Small-scale volcanic systems are the most widespread type of volcanism on Earth and occur in all of the main tectonic settings. Most commonly, these systems erupt basaltic magmas within a wide compositional range from strongly silica undersaturated to saturated and oversatu- rated; less commonly, the spectrum includes more siliceous compositions. Small-scale volcanic systems are commonly monogenetic in the sense that they are represented at the Earth’s surface by fields of small volcanoes, each the product of a temporally restricted eruption of a composition- ally distinct batch of magma, and this is in contrast to polygenetic systems characterized by rela- tively large edifices built by multiple eruptions over longer periods of time involving magmas with diverse origins. Eruption styles of small-scale volcanoes range from pyroclastic to effusive, and are strongly controlled by the relative influence of the characteristics of the magmatic system and the surface environment. Gold Open Access: This article is published under the terms of the CC-BY 3.0 license. Small-scale basaltic magmatic systems characteris- hazards associated with eruptions, and this is tically occur at the Earth’s surface as fields of small particularly true where volcanic fields are in close monogenetic volcanoes. These volcanoes are the proximity to population centres.
    [Show full text]
  • Lafayette - 800 Grams Nakhlite
    Lafayette - 800 grams Nakhlite Figure 1. Photograph showing fine ablation features Figure 2. Photograph of bottom surface of Lafayette of fusion crust on Lafayette meteorite. Sample is meteorite. Photograph from Field Museum Natural shaped like a truncated cone. This is a view of the top History, Chicago, number 62918. of the cone. Sample is 4-5 centimeters across. Photo- graph from Field Museum Natural History, Chicago, number 62913. Introduction According to Graham et al. (1985), “a mass of about 800 grams was noticed by Farrington in 1931 in the geological collections in Purdue University in Lafayette Indiana.” It was first described by Nininger (1935) and Mason (1962). Lafayette is very similar to the Nakhla and Governador Valadares meteorites, but apparently distinct from them (Berkley et al. 1980). Lafayette is a single stone with a fusion crust showing Figure 3. Side view of Lafayette. Photograph from well-developed flow features from ablation in the Field Museum Natural History, Chicago, number Earth’s atmosphere (figures 1,2,3). The specimen is 62917. shaped like a rounded cone with a blunt bottom end. It was apparently oriented during entry into the Earth’s that the water released during stepwise heating of atmosphere. Note that the fine ablation features seen Lafayette was enriched in deuterium. The alteration on Lafayette have not been reported on any of the assemblages in Lafayette continue to be an active field Nakhla specimens. of research, because it has been shown that the alteration in Lafayette occurred on Mars. Karlsson et al. (1992) found that Lafayette contained the most extra-terrestrial water of any Martian Lafayette is 1.32 b.y.
    [Show full text]
  • Chapter 2 Alaska’S Igneous Rocks
    Chapter 2 Alaska’s Igneous Rocks Resources • Alaska Department of Natural Resources, 2010, Division of Geological and Geophysical Surveys, Alaska Geologic Materials Center website, accessed May 27, 2010, at http://www.dggs.dnr.state.ak.us/?link=gmc_overview&menu_link=gmc. • Alaska Resource Education: Alaska Resource Education website, accessed February 22, 2011, at http://www.akresource.org/. • Barton, K.E., Howell, D.G., and Vigil, J.F., 2003, The North America tapestry of time and terrain: U.S. Geological Survey Geologic Investigations Series I-2781, 1 sheet. (Also available at http://pubs.usgs.gov/imap/i2781/.) • Danaher, Hugh, 2006, Mineral identification project website, accessed May 27, 2010, at http://www.fremontica.com/minerals/. • Digital Library for Earth System Education, [n.d.], Find a resource—Bowens reaction series: Digital Library for Earth System Education website, accessed June 10, 2010, at http://www.dlese.org/library/query.do?q=Bowens%20reaction%20series&s=0. • Edwards, L.E., and Pojeta, J., Jr., 1997, Fossils, rocks, and time: U.S. Geological Survey website. (Available at http://pubs.usgs.gov/gip/fossils/contents.html.) • Garden Buildings Direct, 2010, Rocks and minerals: Garden Buildings Direct website, accessed June 4, 2010, at http://www.gardenbuildingsdirect.co.uk/Article/rocks-and- minerals. • Illinois State Museum, 2003, Geology online–GeoGallery: Illinois State Museum Society database, accessed May 27, 2010 at http://geologyonline.museum.state.il.us/geogallery/. • Knecht, Elizebeth, designer, Pearson, R.W., and Hermans, Majorie, eds., 1998, Alaska in maps—A thematic atlas: Alaska Geographic Society, 100 p. Lillie, R.J., 2005, Parks and plates—The geology of our National parks, monuments, and seashores: New York, W.W.
    [Show full text]
  • Module 7 Igneous Rocks IGNEOUS ROCKS
    Module 7 Igneous Rocks IGNEOUS ROCKS ▪ Igneous Rocks form by crystallization of molten rock material IGNEOUS ROCKS ▪ Igneous Rocks form by crystallization of molten rock material ▪ Molten rock material below Earth’s surface is called magma ▪ Molten rock material erupted above Earth’s surface is called lava ▪ The name changes because the composition of the molten material changes as it is erupted due to escape of volatile gases Rocks Cycle Consolidation Crystallization Rock Forming Minerals 1200ºC Olivine High Ca-rich Pyroxene Ca-Na-rich Amphibole Intermediate Na-Ca-rich Continuous branch Continuous Discontinuous branch Discontinuous Biotite Na-rich Plagioclase feldspar of liquid increases liquid of 2 Temperature decreases Temperature SiO Low K-feldspar Muscovite Quartz 700ºC BOWEN’S REACTION SERIES Rock Forming Minerals Olivine Ca-rich Pyroxene Ca-Na-rich Amphibole Na-Ca-rich Continuous branch Continuous Discontinuous branch Discontinuous Biotite Na-rich Plagioclase feldspar K-feldspar Muscovite Quartz BOWEN’S REACTION SERIES Rock Forming Minerals High Temperature Mineral Suite Olivine • Isolated Tetrahedra Structure • Iron, magnesium, silicon, oxygen • Bowen’s Discontinuous Series Augite • Single Chain Structure (Pyroxene) • Iron, magnesium, calcium, silicon, aluminium, oxygen • Bowen’s Discontinuos Series Calcium Feldspar • Framework Silicate Structure (Plagioclase) • Calcium, silicon, aluminium, oxygen • Bowen’s Continuous Series Rock Forming Minerals Intermediate Temperature Mineral Suite Hornblende • Double Chain Structure (Amphibole)
    [Show full text]
  • Pyroclastic Flow Hazards
    Pyroclastic Flow Hazards Lecture Objectives -definition and characteristics -generation of pyroclastic flows -impacts and hazards What are pyroclastic flows? Pyroclastic flows are high- density mixtures of hot, dry rock fragments and hot gases that move away from the vent that erupted them at high speeds. Generation Mechanisms: -explosive eruption of molten or solid rock fragments, or both. -non-explosive eruption of lava when parts of dome or a thick lava flow collapses down a steep slope. Most pyroclastic flows consist of two parts: a basal flow of coarse fragments that moves along the ground, and a turbulent cloud of ash that rises above the basal flow. Ash may fall from this cloud over a wide area downwind from the pyroclastic flow. Mt. St. Helens Effects of pyroclastic flows A pyroclastic flow will destroy nearly everything in its path. With rock fragments ranging in size from ash to boulders traveling across the ground at speeds typically greater than 80 km per hour, pyroclastic flows knock down, shatter, bury or carry away nearly all objects and structures in their way. The extreme temperatures of rocks and gas inside pyroclastic flows, generally between 200°C and 700°C, can cause combustible material to burn, especially petroleum products, wood, vegetation, and houses. Pyroclastic flows vary considerably in size and speed, but even relatively small flows that move <5 km from a volcano can destroy buildings, forests, and farmland. On the margins of pyroclastic flows, death and serious injury to people and animals may result from burns and inhalation of hot ash and gases. Pyroclastic flows generally follow valleys or other low-lying areas and, depending on the volume of rock debris carried by the flow, they can deposit layers of loose rock fragments to depths ranging from less than one meter to more than 200 m.
    [Show full text]
  • The Science Behind Volcanoes
    The Science Behind Volcanoes A volcano is an opening, or rupture, in a planet's surface or crust, which allows hot magma, volcanic ash and gases to escape from the magma chamber below the surface. Volcanoes are generally found where tectonic plates are diverging or converging. A mid-oceanic ridge, for example the Mid-Atlantic Ridge, has examples of volcanoes caused by divergent tectonic plates pulling apart; the Pacific Ring of Fire has examples of volcanoes caused by convergent tectonic plates coming together. By contrast, volcanoes are usually not created where two tectonic plates slide past one another. Volcanoes can also form where there is stretching and thinning of the Earth's crust in the interiors of plates, e.g., in the East African Rift, the Wells Gray-Clearwater volcanic field and the Rio Grande Rift in North America. This type of volcanism falls under the umbrella of "Plate hypothesis" volcanism. Volcanism away from plate boundaries has also been explained as mantle plumes. These so- called "hotspots", for example Hawaii, are postulated to arise from upwelling diapirs with magma from the core–mantle boundary, 3,000 km deep in the Earth. Erupting volcanoes can pose many hazards, not only in the immediate vicinity of the eruption. Volcanic ash can be a threat to aircraft, in particular those with jet engines where ash particles can be melted by the high operating temperature. Large eruptions can affect temperature as ash and droplets of sulfuric acid obscure the sun and cool the Earth's lower atmosphere or troposphere; however, they also absorb heat radiated up from the Earth, thereby warming the stratosphere.
    [Show full text]
  • Mineralogy and Paragenesis of Amphiboles from Gibson Peak Pluton
    THE AIVIERICAN MINERALOGIST, VOL. 49, SEPTEMBER-OCTOBER. 1964 MINERALOGY AND PARAGENESIS OF AMPHIBOLES FROM GIBSON PEAK PLUTON. NORTHERN CALIFORNIA PBrBn W. Lrelrlx, U. S. Geotogi,calSurvey, Denaer,Colorad,o. Ansrnacr Ixrnooucrrow Gibson Peak pluton, a 3-squaremile compositeintrusion in the Trin- itv Aips of northern california, is particularly suitablefor investigation of relations between amphibole paragenesisand igneouscrystallization becauseseveral distinctive amphiboles are important constituents of geneticallyrelated rocks that range from gabbro to trondhjemitic tona- lite. This paper describesthe sequenceof amphibole crystallization in difierent parts of the intrusion and reiates the compositionsof three newly analyzedamphiboles to crystallizationsequence and composition of the enclosingrock. The main conclusionis that compositionsof the investigatedamphiboles are as dependenton time of crystallizationwithin their respectiverocks as on bulk rock composition. Pnrnocn.q.pnrcrNtrnpnBTATroN oF THE Alrpnrsolr panecnNpsrs The generalstructural and petrologicfeatures of Gibson peak pluton are describedelsewhere (Lipman, 1963),and onl1-relations bearing on the origin of the amphibolesare summarizedhere. The pluton is com- posite,and five discreteintrusive units have beenrecognized on the basis of field relations.rn order of intrusion theseare hypersthene-hornblende gabbro, (augite-)hornblendegabbro, hornblende diorite, porphyritic quartz-bearingdiorite, and trondhjemitic biotite tonalite. All units show intrusive contacts with the preceding rocks, are petrographically dis- tinctive, and contain at least one amphibole. An interpretation of th" peak complex paragenesisof the Gibson amphiboles,based mainly on the textural featuresdescribed below, is presentedin Fig. 1. The evi- denceis clear orr the occurrenceof the indicated reactions,but the rela- 1321 PETER W. LIPMAN I I I F I I F I 1 I I cd d l :d d9 z z t.i r F-] {Fl z z.zt- z .=l il.
    [Show full text]
  • Geological Mapping, Structural Setting and Petrographic Description of the Archean Volcanic Rocks of Mnanka Area, North Mara
    PROCEEDINGS, 43rd Workshop on Geothermal Reservoir Engineering Stanford University, Stanford, California, February 12-14, 2018 SGP-TR-213 Geological Mapping, Structural Setting and Petrographic Description of the Archean Volcanic Rocks of Mnanka Area, North Mara Ezra Kavana Acacia Mining PLc, North Mara Gold Mine, Department of Geology, P. O. Box 75864, Dar es Salaam, Tanzania Email: [email protected] Keywords: Musoma Mara Greenstone Belt, Mnanka volcanics, Archaean rocks and lithology ABSTRACT The Mnanka area is situated within the Musoma Mara Greenstone Belt, the area is near to Nyabigena, Gokona and Nyabirama gold mines. Mnanka area comprises of the sequence of predominant rhyolitic volcanic rocks, chert and metasediments. Gold mineralizations in Mnanka area is structure controlled and occur mainly as hydrothermal disseminated intrusion related deposits. Hence the predominant observed structures are joints and flow banding. Measurements from flow banding plotted on stereonets using win-TENSOR software has provided an estimate for the general strike of the area lying 070° to 100° dipping at an average range angle of 70° to 85° while data from joints plotted on stereonets suggest multiple deformation events one of which conforms to the East Africa Rift System (striking WSW-ENE, NNE-SSW and N-S). 1. INTRODUCTION This paper focuses on performing a systematic geological mapping and description of structures and rocks of the Mnanka area. The Mnanka area is located in the Mara region, Tarime district within the Musoma Mara Greenstone Belt. The gold at Mnanka is host ed by volcanic rocks that belong to the Musoma Mara Greenstone Belt (Figure 1). The Mnanka volcanics are found within the Kemambo group that comprises of the sequence of predominant rhyolitic volcanic rocks, chert and metasediments south of the Nyarwana fault.
    [Show full text]