Nativitat (from Latin nativus, meaning ‘born’ or ‘natural’) carries two distinct but related meanings across the Earth sciences. Understanding the difference between its mineralogical and geochronological applications is essential for any geologist, student, or researcher working in petrology, economic geology, or isotope geochemistry.
In its most common usage, Nativitat describes the natural occurrence of chemical elements in their pure, uncombined elemental form within the Earth’s crust these are called native elements or native element minerals. In a more specialized scientific context, the term has been adopted in geochronology to describe a specific property of radiogenic lead systems used in uranium-lead age dating.
Mineralogical Nativitat Native Element Minerals
Native element minerals are chemical elements that occur naturally in a relatively pure or alloyed state, without combining with other elements to form compounds. This is the primary meaning of Nativitat as used in classical mineralogy and economic geology.
Native elements are subdivided into three major groups: metals (e.g., gold, silver, copper, platinum), semi-metals (e.g., arsenic, bismuth, antimony), and non-metals (e.g., sulfur, carbon as diamond or graphite). Although most elements in the Earth’s crust exist as chemical compounds silicates, oxides, sulfides a select few are stable enough in their elemental state to persist under natural geological conditions.
The occurrence of native elements is often controlled by oxidation-reduction (redox) conditions in the environment. Elements with low reactivity or those stabilized by specific pressure-temperature-chemical conditions can remain in their native state. Gold is the classic example: its noble character makes it virtually inert under surface conditions, allowing it to persist as native gold nuggets in stream placers for millions of years.
Geochronological Nativitat Proportion of Radiogenic Lead
In geochronology specifically uranium-lead (U-Pb) and lead-lead (Pb-Pb) isotopic dating Nativitat has been defined as the proportion of radiogenic lead that has been retained within a mineral system since its crystallization or closure. This definition was formally articulated by Ludwig (1998) in the context of lead isotope systematics and age calculation software.
When a uranium-bearing mineral (such as zircon, monazite, or baddeleyite) crystallizes, it incorporates uranium but excludes most lead. Over geological time, uranium decays through two radioactive chains (238U to 206Pb and 235U to 207Pb), generating radiogenic lead. The Nativitat value essentially the proportion of lead that remained in the system undisturbed is critical for determining an accurate crystallization age.
A Nativitat of 1.0 (or 100%) indicates a closed system where all radiogenic lead has been retained: this yields a concordant, reliable age. A Nativitat lower than 1.0 indicates lead loss through metamorphism, hydrothermal alteration, or diffusion, resulting in discordant age determinations. Correcting for common (non-radiogenic) lead and understanding Nativitat is therefore a fundamental step in obtaining accurate geochronological data.
Key Definition (Ludwig, 1998): Nativitat is the proportion of radiogenic lead remaining within a uranium-bearing mineral system a value of 1.0 indicates complete retention (closed system); values below 1.0 indicate partial lead loss.
Complete List of Native Elements & Their Properties
Native elements span a remarkable range of physical and chemical properties. The table below summarizes the most important native elements found in geological contexts, organized by class.
| Element | Symbol | Crystal System | Mohs Hardness | Density (g/cm3) | Key Occurrence |
| Gold | Au | Isometric (cubic) | 2.5 – 3 | 15.6 – 19.3 | Hydrothermal veins, placers |
| Silver | Ag | Isometric (cubic) | 2.5 – 3 | 10.1 – 11.1 | Hydrothermal veins, oxidation zones |
| Copper | Cu | Isometric (cubic) | 2.5 – 3 | 8.9 | Basaltic lavas, hydrothermal |
| Platinum | Pt | Isometric (cubic) | 4 – 4.5 | 21.4 | Mafic/ultramafic intrusions |
| Iron (Meteoric) | Fe | Isometric | 4 – 5 | 7.3 – 7.9 | Meteorites, impact structures |
| Mercury | Hg | Liquid at room T | — | 13.5 | Near volcanic vents, cinnabar zones |
| Arsenic | As | Trigonal | 3.5 | 5.7 | Hydrothermal, near sulfide deposits |
| Bismuth | Bi | Trigonal | 2 – 2.5 | 9.7 – 9.8 | High-temp hydrothermal veins |
| Sulfur | S | Orthorhombic | 1.5 – 2.5 | 2.0 – 2.1 | Volcanic fumaroles, sedimentary |
| Diamond (C) | C | Isometric (cubic) | 10 | 3.5 | Kimberlite pipes, placers |
| Graphite (C) | C | Hexagonal | 1 – 2 | 2.1 – 2.3 | Metamorphic rocks, pegmatites |
Metals Gold, Silver, Copper, Platinum, Iron
Native metals are characterized by their metallic luster, high density, excellent malleability and ductility, and strong electrical and thermal conductivity. Gold is the most chemically stable, owing to its filled d-electron shells and relativistic contraction effects. Native silver is slightly more reactive and commonly oxidizes at the surface, producing a dark tarnish of silver sulfide. Native copper, while reactive, is preserved in reducing environments within basaltic lavas and beneath oxidation zones in sulfide deposits.
Platinum-group elements (PGEs) including platinum, palladium, osmium, iridium, ruthenium, and rhodium occur natively in ultramafic and mafic igneous rocks as part of magmatic segregation processes. They are often found as alloys: osmiridium (Os-Ir), iridosmine (Ir-Os), and platinum-iron alloys. Native iron occurs primarily in meteorites (as the kamacite-taenite intergrowths of iron-nickel) but has also been identified in terrestrial basaltic rocks under highly reducing conditions.
Semi-Metals & Non-Metals Sulfur, Carbon, Arsenic, Bismuth
Semi-metals such as arsenic and bismuth occur natively in hydrothermal environments, typically associated with sulfide mineral assemblages. Native arsenic displays a characteristic garlic odor when struck and has a trigonal crystal structure with a metallic-gray color and submetallic luster. Bismuth, one of the heaviest non-radioactive elements, forms distinctive hopper crystals and is recovered as a by-product of lead and copper smelting.
Carbon is remarkable in that it forms two entirely different native element minerals depending on pressure and temperature: diamond under extreme high-pressure conditions (typically in the mantle, transported to surface via kimberlite pipes) and graphite under lower-pressure metamorphic conditions. Sulfur crystallizes natively around volcanic fumaroles and in evaporite sedimentary environments, forming beautiful yellow orthorhombic crystals with a resinous to adamantine luster.
How Do Native Elements Form?
The formation of native elements depends on specific geochemical conditions particularly the oxidation-reduction (redox) state of the environment, temperature, pressure, and the availability of complexing agents for element transport. The following four geological processes account for the vast majority of native element occurrences worldwide.
Magmatic Segregation
Magmatic segregation refers to the physical and chemical separation of mineral phases during the cooling and solidification of magma. Platinum-group elements (PGEs) and native iron are the primary products of this process. As mafic and ultramafic magmas cool, immiscible sulfide melts form and scavenge PGEs from the silicate melt, concentrating them into discrete sulfide mineral layers. World-class examples include the Bushveld Igneous Complex in South Africa (home to the Merensky Reef, the world’s richest PGE deposit) and the Norilsk-Talnakh district in Russia.
Native iron can crystallize from highly reducing magmas, particularly basalts intruding into coal-bearing sequences where carbon reduces ferrous iron to the metallic state. The Disko Island basalts of Greenland contain well-documented native iron formed in this way.
Hydrothermal Veins
Hydrothermal systems circulating hot, aqueous fluids driven by magmatic or geothermal heat are the single most important environment for the concentration of native gold, silver, copper, arsenic, and bismuth. These fluids transport dissolved metals as chloride or sulfur complexes. When pressure drops, temperature decreases, or the fluid encounters a chemical reaction, gold and silver precipitate from solution.
In epithermal systems (shallow crustal depths of 1–5 km), gold and silver are deposited from low-temperature fluids in quartz veins, commonly associated with adularia and carbonate minerals. In mesothermal or orogenic gold systems (greater crustal depths), gold precipitates in quartz-carbonate-sulfide veins under higher pressure-temperature conditions. The Mother Lode Belt of California and the Kalgoorlie Superpit in Western Australia are classic examples of orogenic gold hosted in hydrothermal veins.
Placer Deposits & Weathering
Native elements with exceptional chemical stability chiefly gold, platinum, and osmium-iridium survive prolonged weathering and mechanical transport to accumulate in placer deposits. As primary ore deposits are weathered and eroded, dense, inert native metal grains are liberated and concentrated by gravity in stream beds, beaches, and ancient alluvial fans.
The supergene enrichment zone, developed immediately above the water table in sulfide deposits, can also produce native copper and native silver through reduction of downward-percolating oxidized solutions. Native copper produced in this way at the Keweenaw Peninsula (Michigan, USA) was mined by Native Americans for thousands of years before European colonization and later became the focus of one of the world’s earliest major copper mining districts.
Reduction Environments
Native copper has a unique and well-documented occurrence in basaltic lava flows, where it forms through the reaction between cupriferous hydrothermal fluids and reducing conditions created by carbonaceous material or ferrous iron in the basalt. The copper is deposited in vesicles, amygdules, and fractures as spectacular dendritic, arborescent, and massive masses. Native sulfur forms in reduction zones near volcanic fumaroles where hydrogen sulfide gases oxidize partially under low-oxygen conditions.
Nativitat in Geochronology Calculating Radiogenic Lead
The geochronological application of Nativitat is more specialized but scientifically critical. It arises in the context of uranium-lead and lead-lead isotopic dating, where the distinction between common (non-radiogenic) and radiogenic lead must be carefully quantified to extract meaningful geological ages.
Why Nativitat Matters for Age Dating
Every uranium-bearing mineral incorporates a small amount of common lead at the time of crystallization. This common lead has its own isotopic composition (a mix of 204Pb, 206Pb, 207Pb, and 208Pb), inherited from the crustal environment. Over geological time, additional 206Pb and 207Pb are generated by radioactive decay of 238U and 235U respectively. The total measured lead in the mineral is therefore a mixture of common lead and radiogenic lead.
To calculate an accurate age, geochronologists must apply a ‘common lead correction’ subtracting the contribution of common lead from the measured totals. The Stacey-Kramers model (1975) provides a widely used framework for estimating the isotopic composition of common lead as a function of geological age. The Nativitat parameter quantifies how much of the radiogenic lead produced since crystallization has been retained in the mineral it is central to interpreting whether an age is primary (reflecting crystallization) or has been disturbed by later thermal or fluid events.
Step-by-Step Calculation Example
Consider a zircon grain analyzed by TIMS (Thermal Ionization Mass Spectrometry) with the following measured isotope ratios:
| Parameter | Symbol | Measured Value |
| 206Pb/238U ratio | r1 | 0.0521 |
| 207Pb/235U ratio | r2 | 0.3687 |
| 207Pb/206Pb ratio | r3 | 0.0517 |
| 204Pb (common Pb monitor) | 204Pb | 0.0000032 (counts) |
| Common Pb 206/204 (Stacey-Kramers) | SK | 18.42 |
Step 1 Estimate common lead contribution: Using the Stacey-Kramers model for the approximate age of the sample (~550 Ma), the common lead 207Pb/206Pb ratio is approximately 0.840. Multiply the measured 204Pb count by the model common 206Pb/204Pb ratio to derive the common 206Pb component.
Step 2 Subtract common lead: Subtract the calculated common 206Pb and 207Pb from the total measured values to yield the purely radiogenic 206Pb* and 207Pb* components.
Step 3 Calculate Nativitat: Nativitat = (measured radiogenic Pb retained) / (total radiogenic Pb produced since crystallization). If the zircon is concordant (Nativitat = 1.0), the 206Pb*/238U and 207Pb*/235U ages will agree within analytical uncertainty, plotting on the Concordia curve.
Step 4 Interpret the result: A zircon with Nativitat < 1.0 has lost some radiogenic lead its data point will plot below the Concordia curve in the Discordant field. The degree of discordance and the direction of the discordia line toward the Concordia curve defines the age of the lead-loss event (usually metamorphism or hydrothermal alteration).
Concordia vs Discordia Visual Interpretation
The Concordia diagram (also called the Wetherill concordia plot) is the standard graphical tool for U-Pb geochronology. The Concordia curve represents the locus of all points where 206Pb*/238U and 207Pb*/235U ages are equal i.e., where Nativitat = 1.0 for both decay systems. A sample plotting on the Concordia curve is termed concordant and yields a reliable, unambiguous crystallization age.
When samples have experienced lead loss, their data points plot below the Concordia curve along a chord called the Discordia line. The upper intercept of the Discordia with the Concordia curve gives the primary crystallization age; the lower intercept gives the age of the lead-loss event. The Isoplot software package (Ludwig, 2003), widely used in geochronological laboratories, automates these calculations and plots the Concordia-Discordia diagram with full uncertainty propagation.
An alternative representation, the Tera-Wasserburg concordia (207Pb/206Pb vs. 238U/206Pb), is preferred for young samples or those with high common lead, such as carbonates and some igneous accessory minerals.
Major Global Deposits of Native Elements
Native element deposits are economically significant and globally distributed. The following section highlights the world’s most important deposits for gold, copper, and platinum-group elements.
Gold Witwatersrand and Carlin Trend
The Witwatersrand Basin of South Africa is the world’s largest gold province, having produced over 50,000 tonnes of gold since mining began in 1886. The gold occurs as native gold in Precambrian conglomerate reefs ancient alluvial placer deposits metamorphosed and compacted into quartzite. Whether the gold is truly detrital (transported as nuggets) or hydrothermal (introduced by later fluids) remains a subject of active scientific debate, though most evidence supports a modified placer origin.
The Carlin Trend of Nevada (USA) hosts one of the world’s richest concentrations of gold deposits, containing invisible gold gold occurring as nanoparticles within arsenian pyrite rather than as visible native gold grains. Other major gold provinces include the Yilgarn Craton (Australia), Superior Province (Canada), Siberian Craton (Russia), and the Guiana Shield (South America).
Copper Keweenaw Peninsula and Cyprus-Type Deposits
The Keweenaw Peninsula of Michigan represents the world’s classic native copper district. Here, native copper was deposited in amygdular basalts and conglomerates of Mesoproterozoic age by hydrothermal fluids circulating through the Midcontinent Rift System. Individual copper masses of several hundred tonnes have been recovered. The deposit was mined extensively from the 1840s through the early 20th century and produced over 10 billion pounds of copper.
Cyprus-type volcanic-massive sulfide (VMS) deposits, originally described from the Troodos ophiolite in Cyprus, contain native copper in their uppermost oxidation zones. VMS deposits form at or near ancient seafloor hydrothermal vents and are important sources of copper, zinc, lead, and gold worldwide.
Platinum Bushveld Complex and Norilsk
The Bushveld Igneous Complex of South Africa contains roughly 80% of the world’s known platinum reserves, concentrated in layered mafic intrusions along the famous Merensky Reef and UG-2 chromitite layers. Platinum occurs as native platinum and as platinum-iron alloys, along with other PGEs in sulfide mineral assemblages. The deposit formed approximately 2.06 billion years ago by magmatic segregation of sulfide-rich liquids.
The Norilsk-Talnakh district in Russia (Siberia) is the world’s largest known nickel-copper-PGE ore deposit, formed by the interaction of mantle-derived flood basalt magmas with crustal sulfur sources. Native platinum and palladium, along with sperrylite (PtAs2) and other PGE minerals, are recovered as by-products of the massive nickel-copper sulfide ores.
How to Identify Native Elements in the Field and Laboratory
Identifying native elements correctly is a foundational skill in field geology and mineralogy. While each native element has unique diagnostic properties, a systematic approach using physical tests in the field can narrow down possibilities rapidly before laboratory confirmation.
Visual and Streak Tests
Gold is immediately recognizable by its characteristic bright yellow color (which does not tarnish), its high density (it feels extraordinarily heavy for its size), and its perfect malleability it can be flattened with a hammer without breaking. It produces a yellow streak. Pyrite (fool’s gold) is brittle, lighter, and produces a black streak a simple streak test distinguishes them instantly.
Native silver has a silver-white metallic luster when fresh but rapidly tarnishes to gray or black. Native copper is copper-red on fresh surfaces, quickly developing a green patina of malachite. Native sulfur is pale yellow with a resinous luster and produces no streak on porcelain.
Hardness and Density Measurements
Hardness testing using the Mohs scale is a rapid field tool. Native gold and silver both have hardness ~2.5, meaning a fingernail (hardness ~2.5) barely scratches them, while a copper coin (hardness ~3) scratches them easily. Diamond, at hardness 10, cannot be scratched by any other mineral. Density measurement using water displacement (Archimedes method) is diagnostic for distinguishing gold (density ~19.3 g/cm3) from pyrite (~5.0 g/cm3) or chalcopyrite (~4.2 g/cm3).
Advanced Laboratory Methods
When field tests are inconclusive, laboratory methods provide definitive identification. Scanning Electron Microscopy with Energy-Dispersive X-ray Spectroscopy (SEM-EDS) provides elemental mapping and point analyses at the micron scale, ideal for identifying fine-grained or invisible native gold in arsenian pyrite. X-ray Fluorescence (XRF) gives bulk elemental compositions rapidly and non-destructively. Electron Probe Microanalysis (EPMA) provides quantitative chemical analyses at high spatial resolution and is the standard method for characterizing native element alloy compositions (e.g., gold-silver ratios in electrum, PGE alloy compositions).
Frequently Asked Questions About Nativitat
Q1: What is the difference between Nativitat and a native element?
Nativitat is the broader concept describing the natural occurrence of elements in their pure or nearly pure elemental state. A native element (or native element mineral) is the specific mineral or substance formed as a result of this natural occurrence. Think of Nativitat as the property and native element as the resulting material.
Q2: How is Nativitat used in uranium-lead dating?
In U-Pb geochronology, Nativitat quantifies the proportion of radiogenic lead retained in a uranium-bearing mineral since crystallization. A Nativitat of 1.0 means all radiogenic lead has been retained (concordant, reliable age); values below 1.0 indicate lead loss through metamorphism or alteration (discordant age). Geochronologists use common lead corrections (e.g., Stacey-Kramers model) to account for non-radiogenic lead and derive accurate ages.
Q3: Which native element is the softest?
Native mercury (Hg) is liquid at room temperature (melting point -39 degrees C) and therefore has no meaningful Mohs hardness. Among solid native elements, graphite is the softest at Mohs 1-2, which is why it is used as pencil lead. Native gold and silver have a Mohs hardness of approximately 2.5.
Q4: Can native elements be alloys?
Yes. Many native elements naturally occur as alloys of two or more elements. Electrum is a natural gold-silver alloy (gold content 20-80%). Osmiridium is a natural osmium-iridium alloy found in placer deposits associated with platinum. Cuprogold and auricupride are natural copper-gold alloys. The IMA (International Mineralogical Association) recognizes specific alloy compositions as distinct mineral species when they meet the criteria of fixed stoichiometry and unique structure.
Q5: What is the most common native element in Earth’s crust?
Carbon, in the form of graphite, is the most volumetrically abundant native element in the Earth’s crust, occurring in metamorphic rocks worldwide. Diamond, the high-pressure polymorph of carbon, is far rarer but more globally recognized. By economic value, native gold is the most significant native element, and platinum-group elements are the most strategically important.
Q6: How do you calculate Nativitat from isotopic data?
Nativitat is calculated by applying a common lead correction (using the Stacey-Kramers model or a two-stage model) to subtract non-radiogenic lead from the measured isotope ratios. The remaining radiogenic lead is compared to the expected radiogenic lead for a given age. Software tools such as Isoplot (Ludwig, 2003) and IsoplotR automate this calculation, applying uncertainty propagation and producing Concordia-Discordia diagrams with statistical best-fit lines.
Q7: Which native elements are found in placer deposits?
Native gold, platinum, and osmium-iridium (osmiridium) are the most common native elements recovered from placer deposits due to their high density, chemical inertness, and resistance to mechanical abrasion during fluvial transport. Native tin (as cassiterite) and diamond are also concentrated in placer settings. The Witwatersrand conglomerate reefs of South Africa represent the world’s largest fossil placer gold deposit.
Conclusion
- Ludwig, K.R. (1998). On the treatment of concordant uranium-lead ages. Geochimica et Cosmochimica Acta, 62(4), 665-676.
- Stacey, J.S. & Kramers, J.D. (1975). Approximation of terrestrial lead isotope evolution by a two-stage model. Earth and Planetary Science Letters, 26(2), 207-221.
- Nesse, W.D. (2011). Introduction to Mineralogy (2nd ed.). Oxford University Press.
- Pirajno, F. (2009). Hydrothermal Processes and Mineral Systems. Springer.
- Faure, G. & Mensing, T.M. (2005). Isotopes: Principles and Applications (3rd ed.). Wiley.
- IMA (International Mineralogical Association) Official mineral list: www.mindat.org
- USGS Mineral Resources Program Deposit maps and economic data: www.usgs.gov/minerals
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