Lab 13 - Introduction to the Geology of the Terrestrial Planets
Total Page:16
File Type:pdf, Size:1020Kb
Load more
Recommended publications
-
Lunar Impact Crater Identification and Age Estimation with Chang’E
ARTICLE https://doi.org/10.1038/s41467-020-20215-y OPEN Lunar impact crater identification and age estimation with Chang’E data by deep and transfer learning ✉ Chen Yang 1,2 , Haishi Zhao 3, Lorenzo Bruzzone4, Jon Atli Benediktsson 5, Yanchun Liang3, Bin Liu 2, ✉ ✉ Xingguo Zeng 2, Renchu Guan 3 , Chunlai Li 2 & Ziyuan Ouyang1,2 1234567890():,; Impact craters, which can be considered the lunar equivalent of fossils, are the most dominant lunar surface features and record the history of the Solar System. We address the problem of automatic crater detection and age estimation. From initially small numbers of recognized craters and dated craters, i.e., 7895 and 1411, respectively, we progressively identify new craters and estimate their ages with Chang’E data and stratigraphic information by transfer learning using deep neural networks. This results in the identification of 109,956 new craters, which is more than a dozen times greater than the initial number of recognized craters. The formation systems of 18,996 newly detected craters larger than 8 km are esti- mated. Here, a new lunar crater database for the mid- and low-latitude regions of the Moon is derived and distributed to the planetary community together with the related data analysis. 1 College of Earth Sciences, Jilin University, 130061 Changchun, China. 2 Key Laboratory of Lunar and Deep Space Exploration, National Astronomical Observatories, Chinese Academy of Sciences, 100101 Beijing, China. 3 Key Laboratory of Symbol Computation and Knowledge Engineering of Ministry of Education, College of Computer Science and Technology, Jilin University, 130012 Changchun, China. 4 Department of Information Engineering and Computer ✉ Science, University of Trento, I-38122 Trento, Italy. -
Timeline of Natural History
Timeline of natural history This timeline of natural history summarizes significant geological and Life timeline Ice Ages biological events from the formation of the 0 — Primates Quater nary Flowers ←Earliest apes Earth to the arrival of modern humans. P Birds h Mammals – Plants Dinosaurs Times are listed in millions of years, or Karo o a n ← Andean Tetrapoda megaanni (Ma). -50 0 — e Arthropods Molluscs r ←Cambrian explosion o ← Cryoge nian Ediacara biota – z ←Earliest animals o ←Earliest plants i Multicellular -1000 — c Contents life ←Sexual reproduction Dating of the Geologic record – P r The earliest Solar System -1500 — o t Precambrian Supereon – e r Eukaryotes Hadean Eon o -2000 — z o Archean Eon i Huron ian – c Eoarchean Era ←Oxygen crisis Paleoarchean Era -2500 — ←Atmospheric oxygen Mesoarchean Era – Photosynthesis Neoarchean Era Pong ola Proterozoic Eon -3000 — A r Paleoproterozoic Era c – h Siderian Period e a Rhyacian Period -3500 — n ←Earliest oxygen Orosirian Period Single-celled – life Statherian Period -4000 — ←Earliest life Mesoproterozoic Era H Calymmian Period a water – d e Ectasian Period a ←Earliest water Stenian Period -4500 — n ←Earth (−4540) (million years ago) Clickable Neoproterozoic Era ( Tonian Period Cryogenian Period Ediacaran Period Phanerozoic Eon Paleozoic Era Cambrian Period Ordovician Period Silurian Period Devonian Period Carboniferous Period Permian Period Mesozoic Era Triassic Period Jurassic Period Cretaceous Period Cenozoic Era Paleogene Period Neogene Period Quaternary Period Etymology of period names References See also External links Dating of the Geologic record The Geologic record is the strata (layers) of rock in the planet's crust and the science of geology is much concerned with the age and origin of all rocks to determine the history and formation of Earth and to understand the forces that have acted upon it. -
Exploring the Bombardment History of the Moon
EXPLORING THE BOMBARDMENT HISTORY OF THE MOON Community White Paper to the Planetary Decadal Survey, 2011-2020 September 15, 2009 Primary Author: William F. Bottke Center for Lunar Origin and Evolution (CLOE) NASA Lunar Science Institute at the Southwest Research Institute 1050 Walnut St., Suite 300 Boulder, CO 80302 Tel: (303) 546-6066 [email protected] Co-Authors/Endorsers: Carlton Allen (NASA JSC) Mahesh Anand (Open U., UK) Nadine Barlow (NAU) Donald Bogard (NASA JSC) Gwen Barnes (U. Idaho) Clark Chapman (SwRI) Barbara A. Cohen (NASA MSFC) Ian A. Crawford (Birkbeck College London, UK) Andrew Daga (U. North Dakota) Luke Dones (SwRI) Dean Eppler (NASA JSC) Vera Assis Fernandes (Berkeley Geochronlogy Center and U. Manchester) Bernard H. Foing (SMART-1, ESA RSSD; Dir., Int. Lunar Expl. Work. Group) Lisa R. Gaddis (US Geological Survey) 1 Jim N. Head (Raytheon) Fredrick P. Horz (LZ Technology/ESCG) Brad Jolliff (Washington U., St Louis) Christian Koeberl (U. Vienna, Austria) Michelle Kirchoff (SwRI) David Kring (LPI) Harold F. (Hal) Levison (SwRI) Simone Marchi (U. Padova, Italy) Charles Meyer (NASA JSC) David A. Minton (U. Arizona) Stephen J. Mojzsis (U. Colorado) Clive Neal (U. Notre Dame) Laurence E. Nyquist (NASA JSC) David Nesvorny (SWRI) Anne Peslier (NASA JSC) Noah Petro (GSFC) Carle Pieters (Brown U.) Jeff Plescia (Johns Hopkins U.) Mark Robinson (Arizona State U.) Greg Schmidt (NASA Lunar Science Institute, NASA Ames) Sen. Harrison H. Schmitt (Apollo 17 Astronaut; U. Wisconsin-Madison) John Spray (U. New Brunswick, Canada) Sarah Stewart-Mukhopadhyay (Harvard U.) Timothy Swindle (U. Arizona) Lawrence Taylor (U. Tennessee-Knoxville) Ross Taylor (Australian National U., Australia) Mark Wieczorek (Institut de Physique du Globe de Paris, France) Nicolle Zellner (Albion College) Maria Zuber (MIT) 2 The Moon is unique. -
Rare Earth Elements in Planetary Crusts: Insights from Chemically Evolved Igneous Suites on Earth and the Moon
minerals Article Rare Earth Elements in Planetary Crusts: Insights from Chemically Evolved Igneous Suites on Earth and the Moon Claire L. McLeod 1,* and Barry J. Shaulis 2 1 Department of Geology and Environmental Earth Sciences, 203 Shideler Hall, Miami University, Oxford, OH 45056, USA 2 Department of Geosciences, Trace Element and Radiogenic Isotope Lab (TRaIL), University of Arkansas, Fayetteville, AR 72701, USA; [email protected] * Correspondence: [email protected]; Tel.: +1-513-529-9662 Received: 5 July 2018; Accepted: 8 October 2018; Published: 16 October 2018 Abstract: The abundance of the rare earth elements (REEs) in Earth’s crust has become the intense focus of study in recent years due to the increasing societal demand for REEs, their increasing utilization in modern-day technology, and the geopolitics associated with their global distribution. Within the context of chemically evolved igneous suites, 122 REE deposits have been identified as being associated with intrusive dike, granitic pegmatites, carbonatites, and alkaline igneous rocks, including A-type granites and undersaturated rocks. These REE resource minerals are not unlimited and with a 5–10% growth in global demand for REEs per annum, consideration of other potential REE sources and their geological and chemical associations is warranted. The Earth’s moon is a planetary object that underwent silicate-metal differentiation early during its history. Following ~99% solidification of a primordial lunar magma ocean, residual liquids were enriched in potassium, REE, and phosphorus (KREEP). While this reservoir has not been directly sampled, its chemical signature has been identified in several lunar lithologies and the Procellarum KREEP Terrane (PKT) on the lunar nearside has an estimated volume of KREEP-rich lithologies at depth of 2.2 × 108 km3. -
Lunar & Planetary Surface Power Management & Distribution
NASA SBIR 2020 Phase I Solicitation Z1.05 Lunar & Planetary Surface Power Management & Distribution Lead Center: GRC Participating Center(s): GSFC, JSC Technology Area: TA3 Space Power and Energy Storage Scope Title Innovative ways to transmit high power for lunar & Mars surface missions Scope Description The Global Exploration Roadmap (January 2018) and the Space Policy Directive (December 2017) detail NASA’s plans for future human-rated space missions. A major factor in this involves establishing bases on the lunar surface and eventually Mars. Surface power for bases is envisioned to be located remotely from the habitat modules and must be efficiently transferred over significant distances. The International Space Station (ISS) has the highest power (100kW), and largest space power distribution system with eight interleaved micro-grids providing power functions similar to a terrestrial power utility. Planetary bases will be similar to the ISS with expectations of multiple power sources, storage, science, and habitation modules, but at higher power levels and with longer distribution networks providing interconnection. In order to enable high power (>100kW) and longer distribution systems on the surface of the moon or Mars, NASA is in need of innovative technologies in the areas of lower mass/higher efficiency power electronic regulators, switchgear, cabling, connectors, wireless sensors, power beaming, power scavenging, and power management control. The technologies of interest would need to operate in extreme temperature environments, including lunar night, and could experience temperature changes from -153C to 123C for lunar applications, and -125C to 80C for Mars bases. In addition to temperature extremes, technologies would need to withstand (have minimal degradation from) lunar dust/regolith, Mars dust storms, and space radiation levels. -
Persistence and Origin of the Lunar Core Dynamo
Persistence and origin of the lunar core dynamo Clément Suaveta,1, Benjamin P. Weissa, William S. Cassatab, David L. Shusterc,d, Jérôme Gattaccecaa,e, Lindsey Chanf, Ian Garrick-Bethellf,g, James W. Headh, Timothy L. Grovea, and Michael D. Fulleri aDepartment of Earth, Atmospheric, and Planetary Sciences, Massachusetts Institute of Technology, Cambridge, MA 02139; bChemical Sciences Division, Lawrence Livermore National Laboratory, Livermore, CA 94550; cDepartment of Earth and Planetary Science, University of California, Berkeley, CA 94720; dBerkeley Geochronology Center, Berkeley, CA 94709; eCentre Européen de Recherche et d’Enseignement des Géosciences de l’Environnement, Centre National de la Recherche Scientifique, Université Aix-Marseille 3, 13545 Aix-en-Provence, France; fDepartment of Earth and Planetary Sciences, University of California, Santa Cruz, CA 95064; gSchool of Space Research, Kyung Hee University, Yongin 446–701, South Korea; hDepartment of Geological Sciences, Brown University, Providence, RI 02912; and iHawai’i Institute of Geophysics and Planetology, University of Hawaii at Manoa, Honolulu, HI 96822 Edited by Neta A. Bahcall, Princeton University, Princeton, NJ, and approved April 16, 2013 (received for review January 22, 2013) The lifetime of the ancient lunar core dynamo has implications for its 10017 as a constraint on the lunar dynamo. Instead, these authors power source and the mechanism of field generation. Here, we report relied on their analyses of 10049, whose subsamples were found to analyses of two 3.56-Gy-old mare basalts demonstrating that they carry a unidirectional magnetization (17) with a seemingly weak were magnetized in a stable and surprisingly intense dynamo mag- paleointensity (4–10 μT). However, our reanalysis of their data netic field of at least ∼13 μT. -
Hadean-Archean Habitability
Hadean - Early Archean: 4.4 to ~ 3.5 Ga How to build a habitable planet? Jack Hills in Australia meta-conglomerat with the oldest minerals on Earth 4.4 Ga Geological time scale 1 : Hadean 2 : Archean Quasi no rock record Rock record First cooling of magma ocean Alteration of basalt to produce serpentinite crust ~ as today on seafloor 146 142 Sm → Nd (T1/2= 103 Ma) silicate/silicate fractionation before total decay of 146Sm ⇒ < 150 Ma, done early Hadean Acasta (Canada) oldest rocks on Earth, end of Hadean, 4.01 Ga Acasta (Canada) oldest rocks on Earth, end of Hadean, 4.01 Ga Acasta (Canada) oldest rocks on Earth, end of Hadean, 4.01 Ga Zircon ages Jack Hills (Australia) meta-conglomerat Archean in age but contains very old zircons Jack Hills (Australia) meta-conglomerat Archean in age but contains very old zircons Jack Hills (Australia) meta-conglomerat Archean in age but contains very old zircons ZrSiO4 1 mm U-Pb age at 4.4 Ga Part of the grain crystalized shortly after end of magma ocean Age distribution of zircons Different dates on different zircon layers Several age populations Oldest Quartz, micas and plagioclase ∂18O in zircons = 5 to 7.4 ‰ Original magma’s = ∂18O ~ 8.5 to 9.5‰ (La/Lu)N zircons⇒(La/Lu)N of magma~ 200 = TTG magma 4.4 Gyr zircons not so different from actual zircons Granitic inclusions present in zircons Quartz, micas and plagioclase ∂18O in zircons = 5 to 7.4 ‰ Original magma’s = ∂18O ~ 8.5 to 9.5‰ (La/Lu)N zircons⇒(La/Lu)N of magma~ 200 = TTG magma 4.4 Gyr zircons not so different from actual zircons Continental -
Venus: Global Warming Gone Bad Earth & Venus: Sister Planets? Venus Earth
Venus: Global warming gone bad Earth & Venus: Sister planets? Venus Earth Mass 5x1024 kg 6x1024 kg a (semi- 0.7 AU 1 AU major axis) What is T at surface ~750 K ~300 K the boiling Temp of water? P at surface ~90 atm ~1 atm atm N2 and H2O CO2 and composition clouds H2SO4 clouds How do we know Venus’s surface temperature? How do we know Venus’s surface temperature? high energy low energy short wavelength long wavelength “bluer” “redder” hot cold How do we know Venus’s surface temperature? the Sun emits light Earth emits light here. T=6000 K here. T=300 K Venus emits light here. T=750 How do we know what the clouds are made of? Spectrum of planet with no atmosphere Amountof light observed above the atmosphere Wavelength of light (in the infrared) How do we know what the clouds are made of? Spectrum of Spectrum of planet with no planet with atmosphere atmosphere Wavelength at which a molecule in the atmosphere absorbs light Amountof light observed above the atmosphere Amountof light observed above the atmosphere Wavelength of light (in the Wavelength of light (in the infrared) infrared) How do we know what the clouds are made of? (Infrared light) How did Venus get so hot? Remember - all gases absorb light at specific wavelengths. “Greenhouse” gases (like carbon dioxide, water and methane) like to absorb in the infrared wavelengths. Planets emit light at infrared wavelengths (same as human bodies). Conclusio n? “Greenhouse” gases don’t lett the heat from the planet escape. -
Why Pluto Is Not a Planet Anymore Or How Astronomical Objects Get Named
3 Why Pluto Is Not a Planet Anymore or How Astronomical Objects Get Named Sethanne Howard USNO retired Abstract Everywhere I go people ask me why Pluto was kicked out of the Solar System. Poor Pluto, 76 years a planet and then summarily dismissed. The answer is not too complicated. It starts with the question how are astronomical objects named or classified; asks who is responsible for this; and ends with international treaties. Ultimately we learn that it makes sense to demote Pluto. Catalogs and Names WHO IS RESPONSIBLE for naming and classifying astronomical objects? The answer varies slightly with the object, and history plays an important part. Let us start with the stars. Most of the bright stars visible to the naked eye were named centuries ago. They generally have kept their old- fashioned names. Betelgeuse is just such an example. It is the eighth brightest star in the northern sky. The star’s name is thought to be derived ,”Yad al-Jauzā' meaning “the Hand of al-Jauzā يد الجوزاء from the Arabic i.e., Orion, with mistransliteration into Medieval Latin leading to the first character y being misread as a b. Betelgeuse is its historical name. The star is also known by its Bayer designation − ∝ Orionis. A Bayeri designation is a stellar designation in which a specific star is identified by a Greek letter followed by the genitive form of its parent constellation’s Latin name. The original list of Bayer designations contained 1,564 stars. The Bayer designation typically assigns the letter alpha to the brightest star in the constellation and moves through the Greek alphabet, with each letter representing the next fainter star. -
405 01.Ps, Page 1-22 @ Normalize ( 405 01.Qxd )
Geological Society of America Special Paper 405 2006 The record of impact processes on the early Earth: A review of the first 2.5 billion years Christian Koeberl† Department of Geological Sciences, University of Vienna, Althanstrasse 14, A-1090 Vienna, Austria ABSTRACT Collisions and impact processes have been important throughout the history of the solar system, including that of the Earth. Small bodies in the early solar system, the planetesimals, grew through collisions, ultimately forming the planets. The Earth started growing ca. 4.56 Ga in this way. Its early history was dominated by violent impacts and collisions, of which we only have circumstantial evidence. The Earth was still growing and had reached ~70%–80% of its present mass when at ca. 4.5 Ga a Mars- sized protoplanet collided with Earth, leading to the formation of the moon—at least according to the currently most popular hypothesis of lunar origin. After its forma- tion, the moon was subjected to intense post-accretionary bombardment between ca. 4.5 and 3.9 Ga. In addition, there is convincing evidence that the Moon experienced an interval of intense bombardment with a maximum at ca. 3.85 ± 0.05 Ga; subsequent mare plains as old as 3.7 or 3.8 Ga are preserved. It is evident that if a late heavy bom- bardment occurred on the Moon, the Earth must have been subjected to an impact flux at least as intense as that recorded on the Moon. The consequences for the Earth must have been devastating, although the exact consequences are the subject of debate (total remelting of the crust versus minimal effects on possibly emerging life forms). -
Planetary Geology: Goals, Future Directions, and Recommendations
NASA Conference Publication 3005 Planetary Geology: Goals, Future Directions, and Recommendations Proceedings of a workshop held at Arizona State University Tempe, Arizona January 1987 NASA Conference Publication 3005 Planetary Geology: Goals, Future Directions, and Recommendations NASA Office of Space Science and Applications Washington, D. C. Proceedings of a workshop held at Arizona State University Tempe, Arizona January 1987 National Aeronautics and Space Administration Scientific and Technical Information Division Preface This report gives results of a workshop on planetary geology held in January, 1987, at Arizona State University at the request of Dr. David Scott, Discipline Scientist, Planetary Geology and Geophysics, NASA. In addition to reviews by the workshop members, it was reviewed by the Planetary Geology and Geophysics Working Group and incorporated comments from Dr. James Underwood, current Discipline Scientist for the program. R. Greeley, January 1988 TABLE OF CONTENTS Page 1.0 Executive Summary ............................................................................... 1 2.0 Introduction ........................................................................................ 3 3.0 Workshop Conclusions ........................................................................... 5 3.1 Planetary geology studies are in transition from a descriptive phase to prcxess-oriented research .................................................. 5 3.2 Quantitative techniques can be applied to existing data. but there is a need for -
Impact Craters on Titan: Finalizing Titan's Crater Population
49th Lunar and Planetary Science Conference 2018 (LPI Contrib. No. 2083) 2105.pdf IMPACT CRATERS ON TITAN: FINALIZING TITAN’S CRATER POPULATION. J. E. Hedgepeth1, C. D. Neish1, E. P. Turtle B. W. Stiles2 1University of Western Ontario Department of Earth Sciences, London, ON ([email protected]), 2Jet Propulsion Laboratory, Pasadena, CA. Introduction: Saturn’s moon Titan is one of the map craters as shapefiles. The craters are meticulously most dynamic bodies in the solar system. It is the only mapped across the surface. This map is compared to the moon with a thick atmosphere, and like Earth’s atmos- most up to date ISS mosaic, updating the crater map phere it has an active hydrological cycle. However, the where necessary. atmosphere of Titan is organic rich and rains methane This finalized catalog of craters on Titan is imported instead of water. As a result, Titan’s surface topography into MATLAB as shapefiles for further analysis. Initial is being modified extensively by many of the same types estimates of crater diameter and center positions are cat- of erosional processes seen on Earth. The methane rain aloged for further work. creates a complex system of river networks, and the Topographic Analysis: Our understanding of im- equatorial regions are covered by seas of organic sand pact cratering controls how we perceive surface changes dunes. on Earth and other worlds. Therefore, constraining cra- The extent of the endogenic and exogenic processes tering processes informs planetary surface evolution. A on Titan is best observed in its impact craters. Impact large catalog of unaltered craters exists on other icy cratering is a fundamental process in planetary geology; worlds that can be compared with those we see on Titan it is a well understood process because of how pervasive [5, 6].