Meteoritics & Planetary Science 47, Nr 4, 453–470 (2012) doi: 10.1111/j.1945-5100.2012.01339.x

Overview of the rocky component of Wild 2 comet samples: Insight into the early solar system, relationship with meteoritic materials and the differences between comets and asteroids

Don BROWNLEE*, Dave JOSWIAK, and Graciela MATRAJT

Department of Astronomy, University of Washington, Seattle, Washington 98195, USA *Corresponding author. E-mail: [email protected] (Received 28 June 2011; revision accepted 17 January 2012)

Abstract–The solid 2–10 lm samples of comet Wild 2 provide a limited but direct view of the solar nebula solids that accreted to form Jupiter family comets. The samples collected by the Stardust mission are dominated by high-temperature materials that are closely analogous to meteoritic components. These materials include chondrule and CAI-like fragments. Five presolar grains have been discovered, but it is clear that isotopically anomalous presolar grains are only a minor fraction of the comet. Although uncertain, the presolar grain content is perhaps higher than found in chondrites and most interplanetary dust particles. It appears that the majority of the analyzed Wild 2 solids were produced in high-temperature ‘‘rock forming’’ environments, and they were then transported past the orbit of Neptune, where they accreted along with ice and organic components to form comet Wild 2. We hypothesize that Wild 2 rocky components are a sample of a ubiquitously distributed flow of nebular solids that was accreted by all bodies including planets and meteorite parent bodies. A primary difference between asteroids and the rocky content of comets is that comets are dominated by this widely distributed component. Asteroids contain this component, but are dominated by locally made materials that give chondrite groups their distinctive properties. Because of the large radial mixing in this scenario, it seems likely that most comets contain a similar mix of rocky materials. If this hypothesis is correct, then properties such as oxygen isotopes and minor element abundances in olivine, should have a wider dispersion than in any chondrite group, and this may be a characteristic property of primitive outer solar system bodies made from widely transported components.

INTRODUCTION meteoritic sample is positively from a comet. The comparison of the Wild 2 samples with inner solar The Stardust mission to comet Wild 2 and the system materials found in chondrites provides a means to Hayabusa mission to the near-Earth asteroid Itokawa directly compare inner and outer solar nebula materials (Yurimoto et al. 2011) provided the only samples that we and constrain models for the origin and mixing of have from specifically known (named) primitive solar nebular solids. The direct sample of the rocky materials system bodies. The Wild 2 samples are the only proven that formed comets at the edge of the solar system samples from a comet, and they are a unique source of provides a level of sample-derived knowledge, analogous information on the solid components that accreted to to ground truth for remote sensing. This information is form planetismals beyond Neptune. Comet samples must particularly insightful for interpreting astronomical data also exist in the interplanetary dust (IDP) and on dust around comets as well as dust around other micrometeorite collections. In the case of IDP collections stars. This overview is focused on a subset of results on targeted on meteor streams, they may be associated with the rocky materials in Wild 2, and is not intended to be a specific comets (Messenger 2002), but unfortunately, it is comprehensive review. It also does not cover the very not presently possible to prove that any particular important results on Wild 2 organics, but good

453 The Meteoritical Society, 2012. 454 D. Brownlee et al. overviews of Wild 2 organics can be found elsewhere JFC, Wild 2 probably experienced multiple outer planet (Sandford et al. 2006; Elsila et al. 2009; Cody et al. 2011; perturbations that led to a planet-to-planet meander that De Gregorio et al. 2011). transferred Wild 2 from beyond Neptune to JFC orbits. This migration period typically lasts a few million years COMET WILD 2 HISTORY (Levison and Duncan 1997). During the active period of such comets, they typically lose about a quarter of their Wild 2 is an active Jupiter family comet (JFC) that radius (Thomas 2009). If Wild 2 is roughly halfway was observed to have at least 20 active jets during the through its JFC lifetime in the inner solar system, it 2004 Stardust flyby (Sekanina et al. 2004). Ground- and should have lost over 200 m of its original surface of space-based measurements indicated a water sublimation rocks, dust, and ice. Before this final phase in the life of rate of 20,000 tons ⁄ day (Farnham and Schleicher 2005, Wild 2, when it passed interior to Neptune’s orbit, it is De Val-Borro et al. 2010) and active emission of CN nearly certain that Wild 2 was stored beyond Neptune (Knight and Schleicher 2010). The spectral emissions of below 50 K for most of the history of the solar system. Wild 2 classify it as a Borrelly-type comet depleted in C2, An interesting complication to understanding the but with average to slightly high NH2 abundance (Fink accretion region of comets is the possibility that planets et al. 1999). This relative depletion of C2 is characteristic and planetismals might have undergone substantial for comets that are believed to have been derived from migration in the early solar system. Both the Nice the Kuiper Belt (A’Hearn et al. 1995). The behavior of Hypothesis (Levison et al. 2011) and the Grand Tack Wild 2 seems to be typical for JFCs, and this comet has Hypothesis (Walsh et al. 2011) propose that the solar an activity level that is much higher than what is likely to system’s planets were originally packed into a region be the average activity level of main belt comets that roughly half the size of the Neptune’s final orbit and that appear to have formed in the asteroid belt and have their redistribution led to major planetismal scattering. A resided there since their origin (Hsieh and Jewitt 2006). recent study by Nesvorny´(2011) even suggests that a The surface of Wild 2 contains km-sized depressions, major planet may have been lost from the early solar some with steep walls and flat floors (Kirk et al. 2005, system. In light of these ideas, the outer solar system ice- Brownlee et al. 2004). Assuming that these are erosional bearing planetismals may have had a more complex features, it is evident that some of the material released origin than traditionally envisioned. by Wild 2 has come from original depths of several hundred meters. Wild 2 also has mesas, pinnacles, and WILD 2 SAMPLE COLLECTION AND roughness on all measurable spatial scales with the LIMITATIONS exception of its overall shape that gives the body a smoothly rounded limb profile. The unusual surface Most of the Wild particles were collected by features (Basilevsky and Keller 2006) indicate that Wild 6.1 km s)1 impact into low-density silica aerogel, but 2 has clearly had a dramatically different evolutionary some were captured by cratering into aluminum foil. The history from other imaged comets or asteroids. If the sample-derived inferences on the nature of comet Wild 2 surface depressions relate to sites of past or present gas are influenced by the sizes of well-preserved particles that and dust emission, then the ubiquitous presence of can be studied. Due to the size distribution of emitted depressions suggest that essentially all of the Wild 2 particles and the size-dependent effects of capture, much surface has emitted dust and rocks into space. of the information on Wild 2 solids comes from a The collected Wild 2 samples were released from an restricted set of materials. Some of the best data come active comet that is presently on a 6-yr orbit with from components in the 2 lm to a few 10 lmin perihelion near the orbit of Mars and aphelion near diameter that were sufficiently strong that they did not Jupiter’s orbit. Prior to 1974, when it made a close flyby fragment during capture in aerogel. Larger components of Jupiter, it was on a 43-year orbit that ranged from are rare, and the smaller ones were selectively degraded Jupiter to beyond Uranus. If Wild 2 is a typical JFC, it during capture due to the combined effects of low should spend 3 · 105 yr on orbits that pass near thermal inertia and intimate contact with molten silica. Jupiter before it is ultimately ejected from the solar Most submicron particles were degraded or even system (Duncan et al. 2004). Typical JFCs spend only dissolved in molten aerogel during the aerogel capture about 7% of this inner solar system time on orbits with process, but a fraction did survive. During impact in perihelia <2.5 AU when they are active enough to be aerogel, weakly bonded materials disaggregated and the generally observable comets (Duncan et al. 2004). separated components were somewhat size-sorted with During the JFC phase, a typical comet may switch about depth. Small components, with large area-to-mass ratios, ten times between orbital periods longer and shorter than tended to stop high in the tracks, while larger 20 yrs (Levison and Duncan 1997). Prior to becoming a components penetrated more deeply before losing their Overview of the rocky component of Wild 2 comet samples 455

Fig. 1. An idealized view of a bulbous entry track caused by a comet particle entering 0.01 g cm)3 silica aerogel flown on the Stardust mission. The particle entered on the right at 6.1 km s)1 and the ‘‘terminal particles’’ are on the left. Most of the submicron components stopped in the hollow bulbous region, a hollow void partly lined by melted silica + projectile. The larger particles that penetrated below the bulb are usually the best-preserved comet samples. The track acts as a sieve size sorting particle components. initial momentum (Fig. 1). The complex process involved in aerogel capture has been discussed elsewhere (Brownlee et al. 2006; Trigo-Rodrı´guez et al. 2008; Niimi et al. 2011). Generally, small isolated components were captured in the upper ‘‘bulb’’ regions of tracks where most of the impact power and aerogel melt were generated. The instantaneous power generated in tracks varies as the cube of the projectile velocity and most of the energy that melts silica aerogel is generated in the upper track regions when the velocity is still high. In most cases, the largest and deepest penetrating components, extending below the bulb, were competent Fig. 2. SEM backscattered electron images of the potted butts strong materials, either mineral grains or solid rocks of five fragments in track 25 made by the CAI-like particle made of multiple phases. nicknamed Inti. All images have the same scale and the The hollow upper bulb regions of tracks are lined fragments that form different parts of the track all have the with melted silica glass that was heated to the silica same basic structure. They are nodules with spinel cores with 1 lm rims of Al-Ti diopside. The entire impacting particle melting point of 1700 C. The thickness of melt lining was composed of these nodules whose internal structures the track should scale with the track diameter and the beautifully preserved during the aerogel capture process. very largest tracks should have equivalent silica glass track liners that are 10 lm thick. Many of the submicron components were in direct contact with micron or larger materials, the integrity of adjacent phases is seen to be masses of molten silica. The solid components larger within a micron of the particle surface. Surfaces were than about 2 lm were generally captured in excellent abraded and lost, but the interiors were preserved in condition and were essentially protected by their thermal excellent state, usually with no discernable thermal inertia (Fig. 2). The effect of this transient heat source is alteration. somewhat analogous to meteorites, where the high The bias in the collection is that much of the finest temperatures generated during atmospheric entry only size fraction and all of the coarsest size fraction were penetrate the thickness of the fusion crust. Sometimes missed, and this hampers comparison of Wild 2 with compressed aerogel also forms a protective cap that other meteoritic materials. While hundreds of submicron insulates a particle during capture, and this process is grains have been studied, the majority of grains in this most effective on large particles because the cap is size were not preserved, and there is no way of thicker. The thermal penetration skin-depth for silicates determining how representative the survivors are. As a collected by Stardust appears to be less than a micron result, the full nature of the submicron fraction remains for the collected samples, although thicker layers of quite uncertain. This is particularly acute for components material may have been lost by melting or vaporization. such as presolar grains and organic materials that are The alteration depth is estimated by observation of the expected to be small. The large components in Wild 2 are perimeter of microtomed particles that show very sharp also uncertain because few particles >100 lm were contact with compressed or aerogel melt. In polyphase collected and the largest samples have yet to be analyzed. 456 D. Brownlee et al.

The electronically measured size distribution of particles is possible that Wild 2 could in fact contain a substantial impacting the leading edge of the spacecraft shows that abundance of full-size chondrules and we would not the bulk of the mass was in millimeter and larger know it because, as previously mentioned, millimeter- particles, but the fluence of millimeter particles was too sized particles are too rare by number to have been small to be sampled by the 0.1 m2 collector. The size sampled even if they do dominate the mass of particles in distribution measured from the Stardust collection (Price the comet’s coma. The size distribution of Wild 2 et al. 2010) combined with particle impact sensor data particles (Price et al. 2010) does not seem to indicate the from the front of the spacecraft indicates that over 90% degree of bimodality that would occur from the of the impacting mass of particles smaller than 700 lm disintegration of a chondrule-rich material similar to diameter was in particles larger than 100 lm. Semarkona. The seriousness of this sampling bias depends on the nature of cometary materials. If larger comet particles COMET SAMPLES AND PRESOLAR GRAINS are just aggregates of many smaller components, then missing the large particles is not a problem. If most of A major surprise of the analysis of Wild 2 samples the large particles are solid components such as has been how ‘‘meteoritic’’ the collected samples are (Ishii chondrules, then it is a major problem. If Wild 2 was et al. 2008). Reasonable pre-mission predictions were composed of materials that generally resembled a that comet solids would be either dominated by well- primitive ordinary chondrite like Semarkona, the preserved interstellar grains or by presolar grains that sampling bias would yield a quite misleading view of the had only been modestly changed by thermal processes in Semarkona parent body because of the dichotomy the solar nebula. A common expectation, as described by between chondrules and fine matrix. Semarkona is Greenberg and Li (1999), was that comet dust should be dominated by tightly packed millimeter chondrules with made of core-mantle interstellar grains composed of fine matrix filling the narrow spaces between them. Most silicate cores surrounded by organic mantles. The silicate of the analyzed particles would be matrix, and the best portion of such grains should be amorphous because the preserved would be those larger than 2 lm. Over 75% of shape of the 10 lm interstellar silicate infrared feature is the mass of Semarkona is in millimeter chondrules that consistent with almost pure amorphous silicates (Kemper would be too rare to impact the Stardust collector. An et al. 2005). Another expectation was that comet dust additional sample consideration is the possibility that might contain appreciable secondary crystalline phases comets may contain components that are systematically that formed in the nebula by subsolidus annealing of retained as surface lag deposits and not be ejected into amorphous silicates at 1000 K. This is the most space. The presence of depressions on Wild 2 that are common explanation for the presence of crystalline over 100 m deep suggests that the development of inert silicates observed in young circumstellar disks (Poteet lag deposits may not be common on this comet and that et al. 2011). It is generally envisioned that the annealing particles released into space may well be representative process could occur in disks either in stable warm disk of the comet’s interior inventory of rocky components. regions (Poteet et al. 2011) or in colder regions, where The abundance of the larger Wild 2 particles that are transient heating can occur due to shocks (Harker and solid competent materials relative to those that are just Desch 2002; Wooden et al. 2007). aggregates of smaller materials is unknown, although Instead of a comet dominated by submicron analysis of solid grains in Stardust tracks has shown a interstellar dust, most of the analyzed Wild 2 materials remarkable abundance of competent grains up to at least that have been examined have been coarser grained and 50 lm size. Burchell et al. (2008) found that essentially appear to be closely related to common meteoritic all the tracks shorter than 100 lm were long thin tracks materials. For the Stardust comet samples described consistent with formation by solid nonfragmenting here, we will use the relative term ‘‘coarse’’ to refer to materials, and that about half of the 1 mm long tracks grains that are larger than a micron or so and much were bulbous-shaped and half were thin. The shorter larger than the size of typical interstellar grains. Most tracks were made by micron-sized particles and the Wild 2 materials formed at high temperature (greater longest ones were made by particles in the 10 lmuptoa than the 1000 K temperature proposed for the annealing few 100 lm size range. The track shapes suggest that the of interstellar amorphous silicates) and, like the major micron-sized particles that made the shorter tracks were meteoritic components, they presumably formed in the coherent, while about half of the 10 lm or larger sized inner solar system. With only a few exceptions, the particles that produced the larger tracks were studied particles are not primary isotopically anomalous fragmenting materials and presumably were either interstellar grains similar to presolar grains (Hoppe 2010) aggregates or otherwise weak or unstable materials. The that have been identified in chondrites (McKeegan et al. nature of the millimeter grains remains unknown, and it 2006, Leitner et al. 2010). To date, five isotopically Overview of the rocky component of Wild 2 comet samples 457 anomalous presolar grains have been found in the micron comet dust, this process did occur in the solar Stardust samples, four in aluminum foil craters (Leitner nebula. In addition to devitrified chondrule glass, there is et al. 2010), and one in an aerogel track (Messenger et al. a component in meteoritic samples that does have a 2009). One of these is a SiC grain and the others are suggested annealing origin. Equilibrated olivine ⁄ glass silicates or oxides. The isotopic compositions of the aggregates are a minor component of interplanetary dust grains fall in the range of similar presolar grains in and their properties are consistent with formation by chondrites. The abundance of these grains in Wild 2 is subsolidus annealing of an amorphous silicate precursor difficult to estimate because particles of the size of (Bradley 1994; Keller and Messenger 2009). interstellar grains (Hoppe 2010) are often degraded during capture. Early findings (Stadermann and Floss CHONDRULES, CAIS, AND MIXING IN THE 2008) indicated that the presolar grain abundance in SOLAR NEBULA Wild 2 might be lower than in primitive chondrites. Later work has shown that thermal degradation during Most of the analyzed Wild 2 particles are either collection has destroyed small grains, and the measured mineral grains or ‘‘rocks’’ composed of multiple phases in presolar grain abundance is now considered to be a the few to 50 lm size range. Many of the Wild 2 rocks are lower limit (Stadermann et al. 2009). With considerable similar to common components in primitive meteorites, uncertainty, the current best estimate is 1400 ppm although they are usually finer-grained than their (Leitner et al. 2010), a value that is higher than the 44– meteoritic counterparts (Hanner and Zolensky 2010). 66 ppm found in the most presolar grain-rich meteorites However, as mentioned previously, these components are and micrometeorites. It is also higher than the 375 ppm coarse relative to presolar grains, and in some cases, they abundance commonly seen in primitive IDPs (Leitner are a million times more massive than typical interstellar et al. 2010). This is, however, less than the 1% presolar grains. Numerous Wild 2 particles have been shown to be grain abundance reported for part of a cluster IDP that either chondrule fragments or chondrule-like fragments is thought to be cometary material (Busemann et al. (Nakamura et al. 2008, 2009; Jacob et al. 2009; Bridges 2009). While isotopically anomalous grain abundances and Changela 2010; Butterworth et al. 2010; Gainsforth may or may not be relatively high in Wild 2 compared et al. 2010; Joswiak et al. 2010, 2012; Ogliore et al. 2012). with chondrites, these presolar grains are still only a very One of these particles even contains a relict 16O-rich minor fraction of the comet’s rocky materials. olivine grain previously made in a 16O-rich reservoir The isotopic compositions of most of the Stardust (Nakamura et al. 2008). samples that have been measured do not support a One of the very first Stardust tracks analyzed was presolar origin. It also does not appear that annealed made by a 20 lm CAI-like particle composed of spinel presolar grains are abundant in Wild 2, at least in the rimmed pyroxene nodules (Simon et al. 2008). This larger than micron size range. In general, most of the particle is 16O-rich like common CAIs and the Sun, and larger than micron particles are too large and too it contains a host of refractory minerals including Al- mineralogically complex to be produced by simple rich, Ti-bearing and Ti-free clinopyroxene, Mg-Al spinel, 1000 K subsolidus annealing of presolar amorphous anorthite, melilite, perovskite, refractory metal, and silicates or clusters of presolar grains (Joswiak et al. osbornite (TiN) grains. Other tracks also contain 2012). The Wild 2 samples contain many components refractory materials, but the abundance of CAIs or even that could not plausibly have formed by solid-state CAI-like particles has not been well determined. It is annealing of presolar material that had roughly solar probably in the range of 1–10%, an abundance that is composition for the rock forming elements. Such lower than CAI-rich chondrites such as Allende, but components include pure forsterite; refractory forsterite much higher than in unequilibrated ordinary chondrites. with high Ca; nearly pure fayalite; LIME olivine with Wild 2 is a potpourri of such remarkably diverse Mn > Fe; sulfides; and minerals such as osbornite, meteoritic materials that it seems unlikely that the comet perovskite, Cr-rich augite, refractory metal inclusions, can be matched to any given chondrite class. The schreibersite, Ti and V-rich pyroxene, and V-rich spinel diversity of mineral compositions even within individual that contain elevated abundances of rather cosmically particles suggests that the Wild 2 samples are at least as rare elements (Hanner and Zolensky 2010, Joswiak et al. primitive as the most primitive type 3.0 chondrites. The 2012). These materials are also found in chondrites, but high Cr content of some Wild 2 olivine grains indicates a their origin is not commonly attributed to annealing of lack of parent body heating beyond what was presolar materials, a simple solid-state process with experienced by type 3.0 chondrites (Grossman and limited potential for producing diverse phases from Brearley 2005). This evidence for the general lack of amorphous interstellar grains. While devitrification does substantial parent body heating is consistent with the not seem to play an important role in making larger than scenario that most of the components released by Wild 2 458 D. Brownlee et al. were simply materials that accreted along with ice and and refractory materials. If the source region of the Wild organics, were stored in ice for the age of the solar 2 grains was in the inner solar system, then the grains system, and then released to space from subsurface must have been transported over distances of 10 AU to regions due to ice sublimation. The presence of abundant reach the region where JFCs accreted. In this scenario, freely released submicron particles in the Wild 2 dust the vast majority of cometary rocky materials, and in coma, that were both detected (Green et al. 2007) and fact the majority of cometary mass, formed in distant collected (Price et al. 2010), practically guarantees that locales and not the Kuiper belt region where the JFCs this comet, or at least its portions released to space, did accreted. This strongly suggests that the cold region of not suffer pervasive internal aqueous or other thermal the solar nebula was a collection site of materials that alteration that would have caused consolidation of fines were made or severely transformed in hot rock-forming into more strongly bonded composites. Although nebular regions. In light of the transportation distances phyllosilicates have not been seen in Wild 2 samples, involved, it seems likely that the materials reaching the there are a number of reports of small amounts of JFC formation region should have been well mixed. As secondary phases that are generally associated with both chondrule and CAI materials were found in the aqueous alteration and these will be discussed later in comet, Wild 2 must have accreted materials that were this article. formed during the time interval when both CAIs and The solar nebula contained multiple regions that chondrules formed or at least existed in the early solar could be considered to be ‘‘rock factories,’’ regions that system. The only Wild 2 sample data that relate to made many of the coarse materials in primitive formation ages are the lack of detection of 26Mg excesses chondrites such as chondrules and CAIs. The millimeter in a CAI fragment (Matzel et al. 2010) and an Fe-rich products of these factories are typically a billion times chondrule fragment (Ogliore et al. 2012). This more massive than typical interstellar dust grains that measurement implies that these two components formed initially delivered rock-forming elements in the early late, after 26Al had decayed or perhaps early, before 26Al solar system. The nebular rock factories did not produce was injected into the solar nebula. meteoritic components by mild processes such as The Wild 2 data imply that particles at least as large subsolidus annealing of presolar grains. They formed as 50 lm were transported radially across the full width new generations of materials under much more extreme of the solar nebula. This transport could have occurred conditions that involved melting, vaporization, and ballistically above the disk or it may have occurred condensation. The most common rock product in the within the plane of the disk. Shu et al. (1996, 2001) solar nebula appears to have been chondrules, nebular predicted that such transport would occur out of the components that commonly formed by episodes of brief plane due to ejection near the Sun by the X-wind. In the heating in the 1400–1750 C range (Hewins and X-wind model, particles as large as CAIs are ejected to Radomsky 1990). The majority of the well-preserved the edge of the solar nebula and beyond by a Wild 2 materials appear to be products of the rock magnetically driven wind that begins just a few radii factories that made the bulk of the materials in from the Sun. Outward transport in the plane has been chondrites. The initial nebular rock-forming episodes modeled by processes involving turbulent diffusion and began with CAI formation and ended a few million years instabilities (Bockelee-Morvan et al. 2002; Keller and later when the last chondrules formed or were reworked. Gail 2004; Ciesla 2007, 2009, 2010; Boss 2008; and Cuzzi Rocks were also made inside strongly heated parent et al. 2008). bodies. Impact debris from aqueous altered, strongly heated and differentiated parent bodies must have joined COMETS AND ASTEROIDS the ensemble of orbiting debris that could spread across the solar nebula and reach the regions where comets It appears that the Wild 2 rocky components are accreted. largely and perhaps entirely composed of material made in distant locales. This situation is totally different from LONG DISTANCE PARTICLE TRANSPORT the case of chondrites. Typical chondrite parent bodies are dominated by local materials whose properties give The results from the Stardust mission provide chondrite classes their distinctive chemical, mineralogical, fundamental information on the mixing of solids larger and isotopic properties. Chondrites do, however, contain than 2 lm in the solar nebula. It appears that the 2– wayfaring materials that did not form locally. These 50 lm size range of Wild 2 rocky materials is dominated materials include presolar grains and CAIs, but they are by materials that formed in 1000–2000 K nebular minor components that are highly diluted by locally environments. They are samples of materials made by made materials. We suggest that a major difference the high-temperature processes that made chondrules between the rocky materials in asteroids and comets is Overview of the rocky component of Wild 2 comet samples 459

Fig. 3. Fe-Mn systematics of olivine in type IIA chondrules from Berlin et al. (2011). The CO ferrous olivines have the most correlated Mn and Fe abundances with a Mn ⁄ Fe less than half of the mean value for primitive ordinary chondrites. The ordinary chondrites (OC) and CR olivines have more complex Mn ⁄ Fe associations, but with distinctive abundance patterns. afu = atomic formula, so Fe in fayalite = 2. that asteroids are dominated by local materials, while concentrations in olivine and high-precision oxygen rocky material in comets is dominated by material from isotope compositions of olivine. Olivine is particularly distant sources. The materials from distant sources are important because it has distinctive properties in somewhat analogous to glacial erratics because their primitive chondrites, and there is a substantial database formation region is unrelated to the location where they of meteoritic data. are found. The work of Berlin et al. (2011), Hewins et al. (2011), Asteroids were close to the rock-forming regions of Zanda et al. (2010), and others has shown that the the solar nebula, and their accretion times were short Mn ⁄ Fe ratios in ferrous olivine (magnesian olivine because of the higher material density and orbital behaves differently) in several chondrite groups are angular velocities in the inner solar system. If the rocky distinctive, as shown in Fig. 3 from Berlin et al. (2011). contents of comets were derived from distant nebular The ferrous olivine in unequilibrated ordinary chondrites materials and transported 10 AU to comet-forming and CO chondrites has well correlated Fe and Mn regions, it is likely that they are a broad and perhaps abundances, but these two groups show distinctively representative sampling of early nebular solids. At a very different Mn ⁄ Fe ratios. The differences may be related to minimum, they should be a representative sampling of condensation, but they can differ among chondrule the nebular component that was widely distributed reservoirs due to loss or gain of either Fe or Mn. CR across the width of the disk. In addition, being the chondrite ferrous olivines have variable Mn ⁄ Fe ratios, dominant source of Kuiper belt rocky materials, this but distinctive distribution pattern with ratios between population is likely to have been accreted on all solar OC and CO chondrites. Unaltered cometary olivine or system bodies, although in the inner solar system it may olivine from any meteoritic source that showed such only have contributed a very minor fraction because of distinctive patterns even for these two elements could not dilution by locally made materials. possibly be a broad sampling of the solar nebula disk. There is a simple way to test the hypothesis that While distinctive properties of chondritic olivine often comets contain a broad mix of nebular materials. If indicate formation from regional or at least restricted comets were made from a broader mix of rocky materials environments, the Wild 2 olivines appear to contain a than those that made individual asteroids, then the broader mix of Mn and other minor element contents difference should be detectable as a broader dispersion of consistent with formation across a broad range of the component properties. Comet solids should contain a early solar system. Wild 2 olivine has a truly broad range broader range of components than found in meteorites of Mn values (Zolensky et al. 2006; Frank and Zolensky from mainbelt asteroids. Specific tracers that could be 2010; Joswiak et al. 2012) and fortunately, the comet used to investigate this difference include minor element contains abundant Fe-rich olivines that can be 460 D. Brownlee et al. meaningfully compared with existing meteoritic and IDP Unfortunately, trying to positively identify GEMS in the data. Ferrous olivines are important because Mn ⁄ Fe is Stardust collection is difficult because GEMS are always not generally correlated in forsteritic olivines. The less than a micron across and such small particles were growing number of minor element analyses of Wild 2 usually strongly heated during capture (Ishii et al. 2008). olivines will provide a way to quantitatively determine Greatly complicating the problem is that the high-speed how the range of olivine grains accreted by Wild 2 aerogel–projectile interaction produces melt glass compare to those that were incorporated into the various (Rietmeijer 2009) with nanometer-sized beads of metal chondrite types. Principal component analyses of such and sulfide that mimic the fundamental interior structure data and comparison with meteoritic data such as that of GEMS. shown in Fig. 3 will shed light on how components from different reservoirs were distributed across the solar AQUEOUS ALTERATION IN COMETS? system. The broad range of properties of specific comet phases, produced in wide ranging nebular environments, Evidence for aqueous alteration is found in the may be the identifying hallmark property of rocky majority of compositionally primitive chondrites. Except cometary matter. for possible cases of formation by thin layers of ‘‘unfrozen Another means of distinguishing different populations water’’ below 0 C, aqueous alteration processes are most of olivine grains is oxygen isotopic composition measured likely to occur in environments with temperatures above at 1 per mil precision. The high-precision oxygen freezing and water vapor partial pressure above isotope data on Mg-rich meteoritic olivine from Libourel 0.006 atm (0.6 kPa), the triple point of water. In early and Chaussidon (2011) indicate that there are solar system history, such environments must have been remarkably distinctive differences at the few per mil level common in the interiors of chondrite parent bodies even between chondrite types, as shown in Fig. 4 from when their blackbody surface temperatures were Libourel and Chaussidon (2011). The implication from <200 K. Heat sources included impacts, heat of this work is that the early solar system had distinctive hydration, and heat from the decay of 26Al. Internal nebular or even planetary reservoirs of material with energy generation from impacts on kilometer-sized bodies somewhat discrete oxygen compositions. Different and radiogenic heating from short-lived radionuclides chondrite types sampled one or more of these reservoirs. should have been lower in the outer solar system because If this interpretation is correct, then high-precision bodies that formed beyond Neptune have lower collision oxygen data might be a straightforward way to detect velocities and their accretion times should be longer. It is material with contributions from the whole disk and not likely that comet assembly did not occur until 26Al had just localized sources. Like minor elements, we would largely decayed. expect O isotopic compositions of a suite of cometary Could liquid water have existed inside comets as olivine to show broader dispersion than found in any small as Wild 2? Wickramasinghe et al. (2009) described chondrite group and should in fact encompass the full a scenario where a strong cometary crust could range of common meteoritic compositions. conceivably contain steady-state pressure above the In addition to measuring the dispersion of properties water triple point and retain liquid water in small of olivine and other phases it is also possible that comets comets, but this model seems contrived. Impacts on may contain unique components that are not found in comets can certainly provide transient conditions where inner solar system materials. If they exist, such water could exist. Contact with liquid water should components could be considered distinctive markers readily transform a loose mix of fine anhydrous phases (smoking guns), whose mere presence would denote into a stronger material containing hydrated silicates, cometary or outer solar system origin. For example, we and perhaps secondary phases such as carbonates and have found at least two materials in both Wild 2 samples magnetite. A strong argument that aqueous alteration and IDPs that have not been reported in chondrites. One has not profoundly altered comets, or at least the is an assemblage of Na,Cr-rich augite, ferrous olivine, materials that they typically release to space, comes from and sometimes albite and spinel (Joswiak et al. 2009), observations of cometary meteor showers. Meteors and the other is a fine-grained assemblage of pyrrhotite, fragment when their strength is exceeded by the dynamic pentlandite, and sphalerite (Joswiak et al. 2012). Other ram pressure of the atmosphere. Meteors associated with distinctive markers might be organic residue from Jupiter Family Comets are the weakest of all meteors sublimed ice or the presence of GEMS, glass with because they have measured crushing strengths of less embedded metal and sulfides. GEMS are an important than 1 kPa, the strength of soft snow (Borovicˇka 2007). component in primitive carbon-rich IDPs (Bradley 1994; This is orders of magnitude weaker than carbonaceous Bradley et al. 1999), but their presence has not been chondrites that have strengths in the 0.3–30 MPa range positively confirmed in other meteoritic samples. (Tsuchiyama et al. 2009). Overview of the rocky component of Wild 2 comet samples 461

Fig. 4. High-precision oxygen isotope compositions of Mg-rich olivine grains in 6 primitive chondrites. The figure from Libourel and Chaussidon (2011) shows data that are consistent with the chondrite groups incorporating olivine from multiple reservoirs with distinctive isotopic compositions. This remarkable data show that the chondrite groups have distinctively different olivine and most contain grains from multiple sources.

All meteorites must be relatively strong rocks to loose aggregate of originally accreted material. In survive atmospheric entry and they are a biased subset of contrast, meteors released by comets fragment into fine meteoroids that are strong and have low entry speed. particles at exceedingly low ram pressures, showing that Their physical strength is much higher than the typical they are weakly bonded porous aggregates. Retention of cometary materials ejected into space by comets, and no its original weakly bonded nature is probably a definitive meteorite can be typical of the unprocessed cometary signature of a truly primitive solar system material that is material that produces meteor showers. The only nearly unmodified since its accretion. Significant aqueous meteoritic analog with the physical strength similar to alteration inside a comet would presumably lithify its cometary meteors are the ‘‘cluster IDPs’’ that fragment contents into strong rocks similar to what has happened into thousands of pieces when they are collected in the in chondrites. stratosphere. Meteorites are strong because they were While comets could have aqueously altered portions compacted and internally bonded by processes of that were formed by processes such as impacts or were thermal metamorphism and ⁄ or aqueous alteration in accreted from larger bodies, it is reasonable to expect their parent bodies. No meteorite is simply a porous that these materials would be inactive and not be ejected 462 D. Brownlee et al. into space by cometary activity. If altered material was were not ejected into space. While phyllosilicates are ejected, then cometary meteor showers would contain often considered to be fine-grained, they are sheet appreciable numbers of strong meteorite-like rocks. silicates and even poorly ordered phyllosilicates found Meteor showers do contain a few hard rocks, but they in chondrites and IDPs usually have coherent regions are rare components (Borovicˇka 2007). It is also unlikely that are microns across. that processed rocks would normally be ejected by Because of the overwhelmingly anhydrous nature of normal cometary activity. The simultaneous release of the >2 lm Wild 2 materials, coupled with the meteor submicron to millimeter comet solids, expelled by strength and the emission of fine solids by comet activity escaping gas, implies that the components did not as discussed previously, we do not believe that Wild 2, or develop strong bonds to one another. For example, if a at least its portions ejected into space, has experienced meteorite like Murchison was soaked in water, frozen, pervasive aqueous alteration in the parent body. Wild 2 and put in a vacuum, it seems unlikely that subliming ice does not resemble meteorites such as Orgueil and would be capable of propelling debris outwards, Murchison that were profoundly transformed by water particularly submicron particles whose surface forces nor does it resemble unequilibrated ordinary chondrites provide strong adhesion to the other surfaces. The that show only moderate evidence for aqueous release of submicron materials from comet rock-ice alteration. A cautionary note here is that the fine-grained mixtures may require individual ice coatings of rocky material that is most sensitive to alteration was not well components even at the submicron level. preserved by the aerogel capture process. Several studies of Wild 2 materials have provided If Wild 2 did not experience large-scale aqueous evidence for phases that are produced by aqueous alteration, but if it does contain bona-fide aqueous alteration. Stodolna et al. (2010) found substantial alteration products, then these materials could have numbers of small magnetite grains in the bulb region either formed in local regions of the comet or on other of track 80. The abundance of these was on the order bodies. Local sources could be impact sites where ice of 10% of the surviving crystalline phases in the melted and produced alteration products. Debris from studied sample. This track is unusual, but it does seem this material could be spread across the comet by reasonable that the magnetite grains have a similar regolith-like processes. If they are produced on other origin to those found in CI and some CM chondrites, bodies and accreted onto Wild 2, they could be and were produced by aqueous alteration. Berger et al. fragments of inner solar materials like carbonaceous (2011) found several small cubanite grains associated chondrite parent bodies or they could also be fragments with pyrrhotite and pentlandite, and suggested that the of substantial size bodies that formed beyond Neptune. association formed by low-temperature aqueous The Kuiper belt contains more bodies >500 km alteration. Hanner and Zolensky (2010) suggested that diameter than exist in the asteroid belt, and it contains the minor amounts of pentlandite seen in Wild 2 are planetary-sized bodies such as the dwarf planets Pluto aqueous alteration products. Small isolated grains of and Eris. There is direct evidence that collisions on these carbonate have been reported (Flynn et al. 2009), but large bodies produce ejected debris that can be accreted small carbonate grains are contaminants in the silica by other bodies in the Kuiper belt region. The 2000 km aerogel and none of the carbonate grains have yet long Haumea appears to be the parent of a collisional been proven to be related to the comet. All of the family of bodies that include high albedo icy and low above reports are rare components whose origin is albedo rocky materials, evidence of the breakup of a consistent with hydrous alteration, but the most body with a rocky interior and ice crust (Brown et al. common aqueous alteration products in chondrites and 2007; Leinhardt et al. 2010). The interiors of large bodies hydrated IDPs are phyllosilicate phases that have not are likely to contain aqueous alteration products, and been found in aerogel tracks (Joswiak et al. 2012) or fragments ejected from impacts on these bodies are likely in Al foil craters (Wozniakiewicz et al. 2010). All of to be contained in all comets. Like meteorites, comets the larger than 2 lm silicate phases that have been are collections of accreted debris and they should contain studied are anhydrous and show no evidence of inclusions of other solar system bodies. Small bodies that alteration by aqueous processes. The Wild 2 samples form by accretion, and are not strongly processed, also contain large numbers of submicron anhydrous should have regolith-like interiors that contain debris silicates that would have been modified by contact from a range of bodies. with water, even for short periods of time. If the comet does contain abundant hydrated silicates, they DIVERSITY AMONG COMETS? would have to have escaped detection because (1) they were mostly of submicron size, (2) they decomposed Assuming that the rocky components of comets are during capture, or (3) they remained in the comet and effectively cosmic sediments that were transported to the Overview of the rocky component of Wild 2 comet samples 463 edge of the solar nebula, we hypothesize that most Evidence against the proposed similarity between comets will commonly contain a similar mix of rocky rocky contents of comets is the Spitzer IR spectra of materials, unless they were transported at different times comet Tempel 1 debris liberated by the Deep Impact or exposed to differing sorting or modification processes. mission. Lisse et al. (2006) interpreted the excellent and Our prediction is that the dust and rock inventories in feature-rich spectrum as a mix of over a dozen different Jupiter Family Comets may be similar due phases. The fit to the comet spectrum included 14% to the mixing processes associated with transportation smecite, several percent each of siderite and magnesite, over distances of tens of astronomical units. Such 15% niningerite, 9% fayalite, 31% forsterite, 17% homogeneity would be in contrast with the inner solar ‘‘amorphous olivine,’’ 33% ferrosilite, 11% diopside, and system, where meteorite parent bodies formed from other phases. Taken at face value, this spectral fitting distinctively different component populations. The great model is a very poor match to the laboratory analytical diversity between meteorite groups is probably related to data on comet Wild 2 samples. There is some overlap, but higher gradients of nebular properties in the inner solar the Tempel 1 mineralogical interpretation is not system and because meteorite parent bodies formed close consistent with Wild 2 or any type of extraterrestrial to regions where rocky components were formed and material that has been analyzed in the laboratory. The reworked by nebular processes. It is also likely that the high abundances of ferrosilite, niningerite, and the high accretion timescale was shorter in the inner solar system fayalite ⁄ forsterite ratio, put Tempel 1 in a unique and that shock-related processes were more likely to category. Unfortunately, there is no sure way to test how have occurred in denser gas and in regions where large meaningful a spectral match to so many phases is without planets were forming. The asteroid region was a complex ground truth, an actual sample return from Tempel 1, or region of the solar nebula because it was near the snow perhaps a landed experiment package that can determine line, Jupiter, the Sun, the regions where chondrules the mineralogy of submicron materials. Comets are formed, and near the boundary between the terrestrial complex mixtures of crystalline, amorphous, and organic and Jovian planets. Dobrica et al. (2009) and Gounelle components with unknown grain sizes, unknown (2011) suggest that there is a continuum between comets relationship between phases, and unknown influence by and asteroids, and this seems likely for the rocky processes such as radiation and shock. Modeling of such a components if comets and asteroids are composed of complex natural material with spectra from a different mixes of basic nebular materials. A multicomponent suite of laboratory standards should be complication to fully exploring this concept is the fact viewed with caution until confirming evidence can be that there are no regions between Jupiter and the Kuiper obtained. In addition to the presence of highly reduced belt where small bodies could be stored for the life of the phases such as niningerite, an issue of major importance is solar system. Original planetesimals in this vast zone whether or not aqueous alteration products such as were all either perturbed elsewhere or were accreted by smectite, magnesite, and siderite really exist in this comet larger bodies. at significant abundance. They have not been found in Astronomical data indicate that there are significant Wild 2 components larger than 2 lm. A weakness of the differences between outer solar system bodies. KBOs comparison of Wild 2 analysis data using well-understood show a spread of spectral reflectance ranging from flat laboratory analysis techniques and the Tempel 1 infrared spectral reflectance (albedo not a function of wavelength) spectra is that the infrared spectrum is emitted by to the reddest bodies in the solar system. These color submicron particles, the size range that is poorly differences may be due to radiation processing of preserved and not reliably characterized in the Stardust condensed volatiles such as H2O, CO2,CH3OH, and collections. If the submicron mineral contents of both NH3, compounds whose abundances can vary comets are similar to each other as well as the mineral mix appreciably with distance in the cold regions of the solar modeled for the Tempel 1 spectra, then the submicron nebula (Brown et al. 2011). Color differences may be fraction of Wild 2 would have to be mineralogically quite related to differences in original volatile contents and not different from the micron and larger components to rocky components. Differences in volatile contents are recovered by the Stardust mission. seen from emission line spectra A’Hearn et al. (1995) and A remarkable aspect of the post-impact Tempel 1 dramatic differences in H2OandCO2 were even seen infrared spectrum is that it is nearly identical to that of from different regions of a single comet, Hartley 2 the bright long period comet Hale Bopp. This implies (A’Hearn et al. 2011). Comet surface images show a that the dust liberated by the impact on the short period remarkable difference in morphology for Jupiter family comet Tempel 1 from the Kuiper belt is similar to the comets (Basilevsky and Keller 2006). In spite of all of dust released by Hale Bopp, an Oort cloud comet that is these observed differences, it is possible that JFCs all eject generally believed to have accreted interior to Neptune’s very similar solid contents. orbit before being ejected into the Oort cloud. The 464 D. Brownlee et al. similarity of Tempel 1 and Hale Bopp IR spectra is The collected meteoritic materials cover a broad notable because short period and long period comets are range of sizes, and while the largest provide the most usually seen to have quite different spectra, indicating a sample mass, the smaller ones provide a sampling of possible difference between these types of comets. Before early solar system materials that is differently and less the impact, Tempel 1 had a typical short period comet influenced by effects related to delivery to Earth-crossing spectrum with only a weak silicate feature above orbits and survival of atmospheric entry. Conventional continuum. After the impact, the spectra changed meteorites are the larger meteoritic materials, but if they dramatically to show a spectrum with very strong are smaller than a millimeter, they are called features, nearly identical to Hale Bopp. This astonishing micrometeorites. The small particles that are collected transformation from the same comet suggests that the before they hit the ground and are numerous enough to apparent differences between long and short period be collected in the stratosphere are called IDPs. Most comets is not a fundamental property of the material meteorites are too strong to be related to typical inside the comet, but is related to the form of the cometary meteoroids whose low strength is determined material that is ejected to space (Hanner and Zolensky by the high altitude fragmentation of material in 2010). The energetic liberation of fine materials from the cometary meteor showers. Rare cometary meteors, or impact produced a spectacular long period comet small fragments of cometary meteors, perhaps hardened spectrum, rich in silicate spectral features, from a short by parent body impacts or aqueous alteration, do have period comet! It is also conceivable that the difference strength similar to chondrites (Borovicˇka 2007), but between the preimpact and postimpact spectra is solely these are uncommon and are not representative of due to profound heterogeneity in the comet. typical material released by comets. Gounelle et al. We have suggested that the rocky components of (2008) discussed the possibility that some fraction of comets may be similar mixtures of materials made in the existing meteorites, including Orgueil, could have formed inner regions of the solar system, but this might not be in the outer solar system. Dobrica et al. (2009) provide true for all comets. Comets like Wild 2 were made when arguments that micrometeorites are cometary and there was a very efficient outward flow, a diffuse ‘‘Grand discuss similarities to Wild 2 samples. Radial Express,’’ that carried material to the region It has long been understood that some of the cosmic beyond Neptune. This radial express is no longer in dust particles collected in the stratosphere must be from operation and it probably did not occur either in the comets, but solar system dust models implied that the first or the final stages of nebular evolution. It is possible majority of collected samples should have asteroidal that the major outflow of dust may have varied with origins (Dermott et al. 2002). A far-reaching change in time and may have either diminished or increased during this view occurred with the model of Nesvorny´et al. transient events such as FU Orionis outbursts. There (2010) that predicts that 85% of IDPs are cometary! This may have been times when the outward flow of inner new and more sophisticated model matches the spatial solar nebula material did not dominate the flux of distribution of infrared emission of the solar system dust presolar grains falling onto the nebula. At such times, cloud observed by the IRAS and other spacecraft. The there might have been comets that formed largely from model also predicts that the long known process of orbital presolar interstellar grains as suggested by Greenberg circularization sufficiently reduces the atmospheric entry and Li (1999)—with their ice and organic coatings speed of comet dust, and thus diminishes a bias intact. It will be an interesting challenge for future hampering atmospheric survival of comet dust on research and future missions to see if the solar system elliptical orbits. Circularization is a process that is did produce two kinds of comets with drastically affected by size, density, optical properties, collisions, different rocky components. resonances, and lifetime as a free orbiting particle. The Nesvorny´et al. model is a radical change from the past WILD 2 MATERIAL AND THE PROVINCE OF and implies that the majority of stratospheric IDPs may METEORITIC SAMPLES be cometary samples. If this is true, then it marks a major sea change in IDP and micrometeorite work and implies Meteoritic materials that have fallen to Earth are that we already have in hand thousands of meteoritic our major source of information on the early solar comet samples from perhaps a significant number of system, but the province of individual samples is usually different comets. This proposition needs to be fully poorly constrained. The Wild 2 samples, from a known explored and exploited because the meteoritic samples active comet, as well as the Itokawa samples returned provide a means to investigate the diversity among comets from an S type asteroid by the Hayabusa mission and leverage mission data to a larger number of bodies (Yurimoto et al. 2011), provide important insight for that can ever be visited by spacecraft. We hope that the relating meteoritic materials to parent bodies. wide dispersion of properties of particular phases, the Overview of the rocky component of Wild 2 comet samples 465 presence of distinctive cometary materials, or other CONCLUSIONS properties can be used to fingerprint comet samples or least provide strong evidence of cometary origin for The laboratory studies of samples from a known specific IDP, micrometeorite, and meteorite samples. comet have provided profound sample-based insight into An extremely important and relatively new aspect of the nature of solid outer solar system materials and how stratospheric cosmic dust collections is the specific they formed. Assuming that the sampled comet is a targeting of collections to occur during the dust plane typical Jupiter family comet, the results paint a quite crossings of specific short period comets (Messenger different picture of how planetesimals formed in the 2002). These targeted collections have been successful outer solar system than was imagined before the Stardust and have returned remarkable samples with mission was flown. Their rocky components, often the exceptionally high presolar grain contents (Busemann majority of their mass, formed in high-temperature et al. 2009 and Floss et al. 2010). Targeted stratospheric nebular environments that were quite distinct from the collections can be effective comet sample return missions environments that produced their icy and organic and cluster IDPs from these flights retain submicron materials. The materials were apparently transported components of the size that were usually destroyed over long distances to environments where they could during aerogel capture on the Stardust mission. accumulate to form ice-rich bodies. The sample results lead to a testable hypothesis that comet Wild 2 solids are WILD 2 SOLIDS AND IMPLICATIONS FOR THE a population of rocky materials that were distributed SURVIVAL OF PRESOLAR ORGANICS across the full breadth of the solar nebula. The hallmark signature of cometary rocky materials may be that they The finding that isotopically anomalous presolar are a diverse set of materials whose nebular-related grains are rare in Wild 2 has profound implications for the properties cover the full range of solids made in the solar survival of presolar organics. If nebular processes nebula. It is reasonable to imagine that the materials that destroyed most of the presolar silicates, they almost surely formed comets were derived from all dust-bearing destroyed most presolar organic materials. It is highly regions of the early solar system. The comet solids are likely that presolar organic and rocky materials were dominated by this component and the same solids are mixed at fine scale and both components should have also found in asteroids that have produced meteorites, experienced the same transport and exposure to but they are highly diluted by locally produced materials. destructive environments. The rocky materials in Wild 2 We also predict that the dust and rocks from other must have been totally devoid of all volatiles after their comets will be similar to those that formed Wild 2 with high temperature origin, and ice and organics must have the caveat that there might be an additional class of become associated with them at a later time. The presence comets that are dominated by presolar grains. Such of ice and organics in comets implies that these comets would have had to have been made during time components formed in quite different environments than periods when inner solar system materials were not the rocky components. If vast quantities of refractory abundantly transported to the edge of the solar system. solids migrated to cold nebular regions, a reasonable If the majority of Kuiper belt bodies were made of the expectation would be that much of ice would have same solids that were found in Wild 2, then it is possible condensed on them when they passed the snow line, the that these broadly distributed high-temperature rocky relatively warm and probably dense region when water materials were also the basic building blocks of larger could first condense to form ice. If this had happened, bodies such as Pluto, Eris, and even Triton, Neptune’s then much of the ice in comets like Wild 2 could have irregular moon that may be a captured Kuiper belt condensed at the highest possible condensation object. An interesting aspect of this speculation is that temperature. If organics coated migrating grains, did they the total mass of these larger KBOs exceeds that total do so before or after ice formation? Ice layers would mass of the asteroid belt by a considerable fraction. The presumably inhibit organic formation by catalytic total mass of meteoritic-like materials that formed in the reactions with nebular CO. If catalytic reactions occurred, solar nebula’s hot ‘‘rock factories’’ and was then ejected they might have had to occur quickly before grains were into cold regions may have been quite substantial. transported to the snow line. Again, a great unknown here If comets that formed at the edge of the solar system is the nature of the cometary submicron fines. Because of are a reasonable proxy for the cold dust seen around their poor preservation, it cannot be shown that the other stars, then the lessons from Wild 2 provide submicron fraction was not loaded with both presolar intriguing insight into the general nature and origin of grains and presolar organics. We can only confidently say circumstellar dust. Formation of silicate materials in hot that these materials were not major materials in the rock-forming regions close to stars may be the dominant >2 lm size fraction. source of circumstellar silicates that are observed to orbit 466 D. Brownlee et al. stars similar to the Sun. Circumstellar crystalline silicates from detailed reviews by Scott Sandford and Brad around stars (Takeuchi and Lin 2002; Van Boeckel et al. DeGregorio. 2004; Oliveira et al. 2011) may have formed by high- temperature nebular processes and then carried outwards Editorial Handling––Dr. Bradley De Gregorio by a massive flow of a second generation of solids made REFERENCES by total transformation of the initial prestellar solid materials accreted from the interstellar medium. Instead A’Hearn M. F., Millis R. L., Schleicher D. G., Osip D. J., and of formation of crystalline material by mild subsolidius Birch P. V. 1995. The ensemble properties of comets: thermal annealing, these solids may have formed by Results from narrowband photometry of 85 comets, processes related to condensation and chondrule 19761992. Icarus 118:223–270. A’Hearn M. F., Belton M. J. S., Delamere W. A., Feaga L. M., formation. These were the major processes that formed Hampton D, Kissel J., Klaasen K. P., McFadden L. A., solids in the Sun’s asteroid region and were the major Meech K. J., Melosh H. J., Schultz P. H., Sunshine J. M., processes that produced the rocky materials that existed Thomas P. C., Veverka J., Wellnitz D. D., Yeomans D. K., in the Kuiper belt region beyond Neptune. Besse S., Bodewits D., Bowling T. J., Carcich B. T., Collins S. The cumulative results of this mission reiterate the M., Farnham T. L., Olivier G., Brendan H., Kelley M. S., Li J.-Y., Lindler D. J., Lisse C. M., McLaughlin S. A., Merlin importance of sample return to primitive bodies. Without F., Protopapa S., Richardson J. E., and Williams J. L. 2011. laboratory studies, often done at the micron and submicron EPOXI at comet Hartley 2. Science 332:1396–1400. scale, such complex materials could not possibly reveal key Basilevsky A. T. and Keller H. U. 2006. Comet nuclei: information such as the abundance of presolar grains and Morphology and implied processes of surface modification. detailed records of early solar system processes. Stardust Planetary and Space Science 54:808–829. Berger E. L., Zega T. J., Keller L. P., and Lauretta D. S. 2011. was limited because of restraints on submicron components Evidence for aqueous activity on comet 81P ⁄ Wild 2 from that complicated the study of organics, presolar grains, and sulfide mineral assemblages in Stardust samples and CI other fine components. The lack of millimeter size chondrites. Geochimica et Cosmochimica Acta 75:3501– components complicates the comparison with meteoritic 3513. components such as chondrules and CAIs. The data from Berlin J., Jones R. H., and Brearley A. J. 2011. Fe-Mn systematics of type IIA chondrules in unequilibrated CO, well-preserved samples clearly show that Wild 2 is an CR and ordinary chondrites. Meteoritics & Planetary unequilibrated object at least as unaltered as type 3.0 Science 46:513–533. chondrites. Wild 2 contains abundant materials that Bockelee-Morvan D., Gautier D., Hersant F., Hure J.-M., and formed at high temperature, but the comet is a very Robert F. 2002. Turbulent radial mixing in the solar nebula primitive body in the sense that it appears to have as the source of crystalline silicates in comets. Astronomy & Astrophysics 384:1107–1118. excellently preserved its originally accreted solids. The Borovicˇka J. 2007. Properties of meteoroids from different evidence that comets are deep-frozen storage facilities of classes of parent bodies. In Near earth objects, our celestial solids formed across the full width of the nebula supports neighbors: opportunity and risk, Proceedings of IAU the importance of future comet sample return missions. Symposium 236, edited by Valsecchi G. B., Vokrouhlicky´ Future missions, with more capability than the Stardust D., and Milani A. Cambridge, UK: Cambridge University Press. pp. 107–120. flyby sample return mission, could collect many orders of Boss A. P. 2008. Mixing in the solar nebula: Implications for magnitude more mass and collect it in a largely isotopic heterogeneity and large-scale transport of nondestructive manner. Such collections, even done at refractory grains. Earth and Planetary Science Letters room temperature, would provide information on organics 268:102–109. and fines and components in the chondrule to CAI size Bradley J. P. 1994. Nanometer-scale mineralogy and petrography of fine-grained aggregates in anhydrous range. Detailed studies of these samples could provide interplanetary dust particles. Geochimica et Cosmochimica unprecedented information on the chronology of nebular Acta 58:2123–2134. materials, their properties, and how they were transported Bradley J. P., Keller L. P., Snow T. P., Hanner M. S., Flynn G. across the solar nebula. They would also provide vital J., Gezo J. C., Clemett S. J., Brownlee D. E., and Bowey J. information on comet diversity and the origin of organic E. 1999. An infrared spectral match between GEMS and interstellar grains. Science 285:1716–1718. matter in comets. Bridges J. C. and Changela H. G. 2010. Chondrule fragments in Stardust tracks 113 and 154 (abstract #5280). Meteoritics Acknowledgments–– We are indebted to NASA for & Planetary Science 45. funding the Stardust mission and its sample analysis Brown M. E., Barkume K. M., Ragozzine D., and Schaller E. program. We are eternally grateful for the efforts put L. 2007. A collisional family of icy objects in the Kuiper belt. Nature 446:294–296. into this endeavor by the entire Stardust mission team Brown M. E., Schaller E. L., and Fraser W. C. 2011. A and the global team of researchers who are analyzing hypothesis for the color diversity of the Kuiper belt. The these unique samples. This contribution greatly benefited Astrophysical Journal 739:L60. Overview of the rocky component of Wild 2 comet samples 467

Brownlee D. E., Ho¨rz F., Newburn R. L., Zolensky M., stardust track C2052,2,74 (abstract #2446). 41st Lunar and Duxbury T. C., Sandford S., Sekanina Z., Tsou P., Hanner Planetary Institute Science Conference. CD-ROM. M. S., Clark B. C., Green S. F., and Kissel J. 2004. Surface Ciesla F. J. 2007. Outward transport of high-temperature of young Jupiter family comet 81 P ⁄ Wild 2: View from the materials around the midplane of the solar nebula. Science Stardust spacecraft. Science 304:1764–1769. 318:613–615. Brownlee D., Tsou P., Aleon J., Alexander C. M. O’D., Araki Ciesla F. J. 2009. Two-dimensional transport of solids in T., Bajt S., Baratta G. A., Bastien R., Bland P., Bleuet P., viscous protoplanetary disks. Icarus 200:655–671. Borg J., Bradley J. P., Brearley A., Brenker F., Brennan S., Ciesla F. J. 2010. Residence times of particles in diffusive Bridges J. C., Browning N. D., Brucato J. R., Bullock E., protoplanetary disk environments. I. Vertical motions. The Burchell M. J., Busemann H., Butterworth A., Chaussidon Astrophysical Journal 723:514–529. M., Cheuvront A., Chi M., Cintala M. J., Clark B. C., Cody G., Heying E., Alexander C. M. O’D., Nittler L. R., Clemett S. J., Cody G., Colangeli L., Cooper G., Cordier Kilcoyne A. L. D., Sandford S. A., and Stroud R. M. 2011. P., Daghlian C., Dai Z., D’Hendecourt L., Djouadi Z., Establishing a molecular relationship between chondritic Dominguez G., Duxbury T., Dworkin J. P., Ebel D. S., and cometary organic solids. Proceedings of the National Economou T. E., Fakra S., Fairey S. A.J., Fallon S., Academy of Sciences 108:19171–19176. Ferrini G., Ferroir T., Fleckenstein H., Floss C., Flynn G., Cuzzi J. N., Hogan R. C., and Shariff K. 2008. Toward Franchi I. A., Fries M., Gainsforth Z., Gallien J.-P., Genge planetesimals: Dense chondrule clumps in the protoplanetary M., Gilles M. K., Gillet P., Gilmour J., Glavin D. P., nebula. The Astrophysical Journal 687:1432–1447. Gounelle M., Grady M. M., Graham G. A., Grant P. G., De Gregorio B. T., Stroud R. M., Cody G. D., Nittler L. R., Green S. F., Grossemy F., Grossman L., Grossman J. N., Kilcoyne A. L. D., and Wirick S. 2011. Correlated Guan Y., Hagiya K., Harvey R., Heck P., Herzog G. F., microanalysis of cometary organic grains returned by Hoppe P., Horz F., Huth J., Hutcheon I. D., Ignatyev K., Stardust. Meteoritics & Planetary Science 46:1376–1396. Ishii H., Ito M., Jacob D., Jacobsen C., Jacobsen S., Jones Dermott S. F., Durda D. D., Grogan K., and Kehoe T. J. J. S., Joswiak D., Jurewicz A., Kearsley A. T., Keller L. P., 2002. Asteroidal Dust. In Asteroids III, edited by Bottke W. Khodja H., Kilcoyne A. L. D., Kissel J., Krot A., F. Jr., Cellino A., Paolicchi P., and Binzel R. P. Tucson, Langenhorst F., Lanzirotti A., Le L., Leshin L. A., Leitner AZ: The University of Arizona Press. pp. 423–442. J., Lemelle L., Leroux H., Liu M.-C., Luening K., Lyon I., De Val-Borro M., Hartogh P., Crovisier J., Bockelee-Morvan MacPherson G., Marcus M. A., Marhas K., Marty B., D., Biver N., Lis D. C., Moreno R., Jarchow C., Rengel Matrajt G., McKeegan K., Meibom A., Mennella V., M., Szutowicz S., Banaszkiewicz M., Bensch F., Blecka M. Messenger K., Messenger S., Mikouchi T., Mostefaoui S., I., Emprechtinger M., Encrenaz T., Jehin E., Kuppers M., Nakamura T., Nakano T., Newville M., Nittler L. R., Lara L.-M., Lellouch E., Swinyard B. M., Vandenbussche Ohnishi I., Ohsumi K., Okudaira K., Papanastassiou D. A., B., Bergin E. A., Blake G. A., Blommaert J. A. D. L., Palma R., Palumbo M. E., Pepin R. O., Perkins D., Cernicharo J., Decin L., Encrenaz P., de Graauw T., Perronnet M., Pianetta P., Rao W., Rietmeijer F. J. M., Hutsemekers D., Kidger M., Manfroid J., Medvedev A. S., Robert F., Rost D., Rotundi A., Ryan R., Sandford S. A., Naylor D. A., Schieder R., Stam D., Thomas N., Waelkens Schwandt C. S., See T. H., Schlutter D., Sheffield-Parker J., C., Szczerba R., Saraceno P., di Giorgio A. M., Philipp S., Simionovici A., Simon S., Sitnitsky I., Snead C. J., Spencer Klein T., Ossenkopf V., Zaal P., and Shipman R. 2010. M. K., Stadermann F. J., Steele A., Stephan T., Stroud R., Water production in comet 81P ⁄ Wild 2 as determined by Susini J., Sutton S. R., Suzuki Y., Taheri M., Taylor S., Herschel ⁄ HIFI. Astronomy & Astrophysics 521:L50–L50. Teslich N., Tomeoka K., Tomioka N., Toppani A., Trigo- Dobrica E., Engrand C., Duprat J., Gounelle M., Leroux H., Rodrı´guez J. M., Troadec D., Tsuchiyama A., Tuzzolino A. Quirico E., and Rouzaud J. N. 2009. Connection between J., Tyliszczak T., Uesugi K., Velbel M., Vellenga J., Vicenzi micrometeorites and Wild 2 particles: From Antarctic snow to E., Vincze L., Warren J., Weber I., Weisberg M., Westphal cometary ices. Meteoritics & Planetary Science 44:1643–1661. A. J., Wirick S., Wooden D., Wopenka B., Wozniakiewicz Duncan M., Levison H., and Dones L. 2004. Dynamical P., Wright I., Yabuta H., Yano H., Young E. D., Zare R. evolution of ecliptic comets. In Comets II, edited by Festou N., Zega T., Ziegler K., Zimmerman L., Zinner E., and M. C., Keller H. U., Weaver H. Tucson, AZ: The Zolensky M. 2006. Comet 81P ⁄ Wild 2 under a microscope. University of Arizona Press. pp. 193–204. Science 314:1711–1716. Elsila J. E., Glavin D. P., and Dworkin J. P. 2009. Cometary Burchell M. J., Fairey S. A. J., Wozniakiewicz P., Brownlee D. glycine detected in samples returned by Stardust. E., Horz F., Kearsley A. T., See T. H., Tsou P., Westphal Meteoritics & Planetary Science 44:1323–1330. A., Green S. F., Trigo-Rodrı´guez J. M., and Dominguez G. Farnham T. L. and Schleicher D. G. 2005. Physical and 2008. Characteristics of cometary dust tracks in Stardust compositional studies of Comet 81P ⁄ Wild 2 at multiple aerogel and laboratory calibrations. Meteoritics & apparitions. Icarus 173:533–558. Planetary Science 43:23–40. Fink U., Hicks M. P., and Fevig R. A. 1999. Production rates Busemann H., Nguyen A. N., Cody G. D., Hoppe P., Kilcoyne for the Stardust mission target: 81P ⁄ Wild 2. Icarus 141:331– A. L. D., Stroud R. M., Zega T. J., and Nittler L. R. 2009. 340. Ultra-primitive interplanetary dust particles from the comet Floss C., Stadermann F. J., Mertz A. F., and Bernatowicz T. J. 26P ⁄ Grigg-Skjellerup dust stream collection. Earth and 2010. A NanoSIMS and Auger Nanoprobe investigation of Planetary Science Letters 288:44–57. an isotopically primitive interplanetary dust particle from Butterworth A. L., Gainsforth Z., Bauville A., Bonal L., the 55P ⁄ Tempel-Tuttle targeted stratospheric dust collector. Brownlee D. E., Fakra S. C., Huss G. R., Joswiak D., Kunz Meteoritics & Planetary Science 45:1889–1905. M., Marcus M. A., Nagashima K., Ogliore R. C., Tamura Flynn G. J., Wirick S., Keller L. P., and Jacobsen C. 2009. N., Telus M., Tyliszczak T., and Westphal A. J. 2010. A STXM search for carbonate in samples of Comet 81P ⁄ Wild Type IIA chondrule fragment from comet 81P ⁄ Wild 2 in 2. Journal of Physics Conference Series 186:012085. 468 D. Brownlee et al.

Frank D. and Zolensky M. 2010. A mineralogical comparison Joswiak D. J., Brownlee D. E., Matrajt G., Messenger S. of Stardust Wild 2 grains and carbonaceous chondrites M., and Ito M. 2010. Stardust track 130 terminal (abstract #5411). Meteoritics & Planetary Science 45. particle: Possible Al-rich chondrule fragment or altered Gainsforth Z., Butterworth A. L., Bonal L., Brownlee D. E., amoeboid olivine aggregate (abstract #2119). 41st Lunar HussG.R.,JoswiakD.,OglioreR.C.,TelusM.,Tyliczszak and Planetary Science Conference. CD-ROM. T., and Westphal A. J. 2010. Coordinated TEM ⁄ STXM ⁄ IMS Joswiak D. J., Brownlee D. E., and Matrajt G. 2012. analysis of a type IIA chondrule fragment from Comet Comprehensive examination of large mineral and rock 81P ⁄ Wild 2 Stardust track C2052,2,74. Meteoritics & fragments in Stardust tracks: Mineralogy, analog Planetary Science Supplement 73:5428. extraterrestrial materials and source regions. Meteoritics & Gounelle M. 2011. The asteroid comet continuum: In search of Planetary Science 47:1–52. lost primitivity. Elements 7:29–34. Keller C. and Gail H.-P. 2004. Radial mixing in protoplanetary Gounelle M., Morbidelli A., Bland P. A., Spurny´P., Young E. accretion disks. VI. Mixing by large-scale radial flows. D., and Sephton M. 2008. Meteorites from the outer solar Astronomy & Astrophysics 415:1177–1185. system? The solar system beyond Neptune. In The solar Keller L. P. and Messenger S. 2009. Equilibrated aggregates in system beyond Neptune, edited by Barucci M.A., cometary IDPs: Insights into the crystallization process in Boehnhardt H., Cruikshank D. P., and Morbidelli A. protoplanetary disks (abstract #2121). 40th Lunar and Tucson, AZ: The University of Arizona Press. pp. 525–541. Planetary Institute Science Conference. CD-ROM. Green S. F., McBride N., Colwell M. T. S. H., McDonnell J. Kemper F., Vriend W. J., and Tielens A. G. G. M. 2005. A. M., Tuzzolino A. J., Economou T. E., Clark B. C., Erratum: ‘‘The Absence of Crystalline Silicates in the Sekanina Z., Tsou P., and Brownlee D. E. 2007. Stardust Diffuse Interstellar Medium.’’ The Astrophysical Journal Wild 2 dust measurements.In Dust in planetary systems, 633:534–534. edited by Krueger H. and Graps A. Workshop on Dust in Kirk R. L., Duxbury T. C., Horz F., Brownlee D. E., Newburn Planetary Systems (ESA SP-643). September 26–30 2005. R. L., and Tsou P. The Stardust Team. 2005. Topography Kauai, Hawaii. Noordwijk, The Netherlands: ESTEC. pp. of the 81 ⁄ P Wild 2 nucleus derived from Stardust 35–44. stereoimages (abstract #2244). Proceedings, 36th Lunar and Greenberg J. M. and Li A. 1999. All comets are born equal: Planetary Science Conference. CD-ROM. Infrared emission by dust as a key to comet nucleus Knight M. M. and Schleicher D. G. 2010. Dust and gas composition. Planetary and Space Science 47:787–795. morphology of Comets 81P ⁄ Wild 2, 10P ⁄ Tempel 2, and Grossman J. N. and Brearley A. J. 2005. The onset of 103P ⁄ Hartley 2. Bulletin of the American Astronomical metamorphism in ordinary and carbonaceous chondrites. Society 42:965. Meteoritics & Planetary Science 40:87–122. Leinhardt Z. M., Marcus R. A., and Stewart S. T. 2010. The Hanner M. S., and Zolensky M. E. 2010. The mineralogy of Formation of the collisional family around the dwarf planet cometary dust. In Lecture notes in physics, vol. 815, edited Haumea. The Astrophysical Journal 714:1789–1799. by Henning T. Berlin: Springer Verlag. pp. 203–232. Leitner J., Hoppe P., and Heck P. R. 2010. First discovery of Harker D. E. and Desch S. J. 2002. Annealing of silicate dust presolar material of possible supernova origin in impact by nebular shocks at 10 AU. The Astrophysical Journal residues from Comet 81P ⁄ Wild 2 (abstract #1607). 41st 565:L109–L112. Lunar and Planetary Science Conference. CD-ROM. Hewins R. H. and Radomsky P. M. 1990. Temperature Levison H. F. and Duncan M. J. 1997. From the Kuiper belt to conditions for chondrule formation. Meteoritics 25:309– Jupiter-family comets: The spatial distribution of ecliptic 318. comets. Icarus 127:13–32. Hewins R. H., Zanda B., and Bourot-Denise M. 2011. The Levison H. F., Morbidelli A., Tsiganis K., Nesvorne D., and formation of Type II chondrules in CM chondrites Gomes R. 2011. Late orbital instabilities in the outer (abstract #1914). 42nd Lunar and Planetary Science planets induced by interaction with a self-gravitating Conference. CD-ROM. planetesimal disk. The Astronomical Journal 142:152–163. Hoppe P. 2010. Stardust in primitive solar system materials. Libourel G. and Chaussidon M. 2011. Oxygen isotopic Proceedings, American Institute of Physics Conference constraints on the origin of Mg-rich olivines from Series 1213, pp. 84–94. chondritic meteorites. Earth and Planetary Science Letters Hsieh H. H. and Jewitt D. 2006. A population of comets in the 301:9–21. main asteroid belt. Science 312:561–563. Lisse C. M., VanCleve J., Adams A. C., A’Hearn M. F., Ishii H. A., Bradley J. P., Dai Z. R., Chi M., Kearsley A. T., Fernandez Y. R., Farnham T. L., Armus L., Grillmair C. Burchell M. J., Browning N. D., and Molster F. 2008. J., Ingalls J., Belton M. J. S., Groussin O., McFadden L. Comparison of comet 81P ⁄ Wild 2 dust with interplanetary A., Meech K. J., Schultz P. H., Clark B. C., Feaga L. M., dust from comets, Science 25:447–450. and Sunshine J. M. 2006. Spitzer spectral observations of Jacob D., Stodolna J., Leroux H., Langenhorst F., and the deep impact ejecta. Science 313:635–640. Houdellier F. 2009. Pyroxenes microstructure in comet Matzel J. E. P., Ishii H. A., Joswiak D., Hutcheon I. D., 81P ⁄ Wild 2 terminal Stardust particles. Meteoritics & Bradley J. P., Brownlee D., Weber P. K., Teslich N., Planetary Science 44:1475–1488. Matrajt G., McKeegan K. D., and MacPherson G. J. 2010. Joswiak D. J., Brownlee D. E., Matrajt G., Westphal A. J., and Constraints on the formation age of cometary material Snead C. J. 2009. Kosmochloric Ca-rich pyroxenes and from the NASA Stardust mission. Science 328:483–486. FeO-rich olivines (Kool grains) and associated phases in McKeegan K. D., Aleon J., Bradley J., Brownlee D., Stardust tracks and chondritic porous interplanetary dust Busemann H., Butterworth A., Chaussidon M., Fallon S., particles: Possible precursors to FeO-rich type II chondrules Floss C., Gilmour J., Gounelle M., Graham G., Guan Y., in ordinary chondrites. Meteoritics & Planetary Science Heck P. R., Hoppe P., Hutcheon I. D., Huth J., Ishii H., 44:1561–1588. Ito M., Jacobsen S. B., Kearsley A., Leshin L. A., Liu Overview of the rocky component of Wild 2 comet samples 469

M.-C., Lyon I., Marhas K., Marty B., Matrajt G., Meibom Sandford S. A., Aleon J., Alexander C. M. O’D., Araki T., A., Messenger S., Mostefaoui S., Mukhopadhyay S., Bajt S., Baratta G. A., Borg J., Bradley J. P., Brownlee Nakamura-Messenger K., Nittler L., Palma R., Pepin R. D. E., Brucato J. R., Burchell M. J., Busemann H., O., Papanastassiou D. A., Robert F., Schlutter D., Snead Butterworth A., Clemett S. J., Cody G., Colangeli L., C. J., Stadermann F. J., Stroud R., Tsou P., Westphal A., Cooper G., D’Hendecourt L., Djouadi Z., Dworkin J. P., Young E. D., Ziegler K., Zimmermann L., and Zinner E. Ferrini G., Fleckenstein H., Flynn G. J., Franchi I. A., 2006. Isotopic compositions of cometary matter returned by Fries M., Gilles M. K., Glavin D. P., Gounelle M., Stardust. Science 314:1724–1728. Grossemy F., Jacobsen C., Keller L. P., Kilcoyne A. L. Messenger S. 2002. Opportunities for the stratospheric D., Leitner J., Matrajt G., Meibom A., Mennella V., collection of dust from short-period comets. Meteoritics & Mostefaoui S., Nittler L. R., Palumbo M. E., Planetary Science 37:1491–1506. Papanastassiou D. A., Robert F., Rotundi A., Snead C. Messenger S., Joswiak D., Ito M., Matrajt G., and Brownlee J., Spencer M. K., Stadermann F. J., Steele A., Stephan D. E. 2009. Discovery of presolar SiC from Comet Wild 2 T., Tsou P., Tyliszczak T., Westphal A. J., Wirick S., (abstract #1790). 40th Lunar and Planetary Science Wopenka B., Yabuta H., Zare R. N., and Zolensky M. Conference. CD-ROM. E. 2006. Organics captured from comet 81P ⁄ Wild 2 by Nakamura T., Noguchi T., Tsuchiyama A., Ushikubo T., Kita the Stardust spacecraft. Science 314:1720. N. T., Valley J. W., Zolensky M. E., Kakazu Y., Sakamoto Sekanina Z., Brownlee D. E., Economou T. E., Tuzzolino A. K., Mashio E., Uesugi K., and Nakano T. 2008. J., and Green S. F. 2004. Modeling the nucleus and jets of Chondrule-like objects in short-period comet 81P ⁄ Wild 2. comet 81P ⁄ Wild 2 based on the Stardust encounter data. Science 321:1664–1667. Science 304:1769–1774. Nakamura T., Noguchi T., Tsuchiyama A., Ushikubo T., Kita Shu F. H., Shang H., and Lee T. 1996. Toward an N. T., Valley J. W., Takahata N., Sano Y., Zolensky M. E., astrophysical theory of chondrites. Science 271:1545–1552. Kakazu Y., Uesugi K., and Nakano T. 2009. Additional Shu F. H., Shang H., Gounelle M., Glassgold A. E., and Lee T. evidence for the presence of chondrules in comet 81P ⁄ 2001. The origin of chondrules and refractory inclusions in Wild 2. (abstract #5304). Meteoritics & Planetary Science chondritic meteorites. The Astrophysical Journal 548:1029– 44. 1050. Nesvorny´D. 2011. Young solar system’s fifth giant planet? The Simon S. B., Joswiak D. J., Ishii H. A., Bradley J. P., Chi M., Astrophysical Journal 742:L22. Grossman L., Aleon J., Brownlee D. E., Fallon S., Nesvorny´D., Jenniskens P., Levison H. F., Bottke W. F., Hutcheon I. D., Matrajt G., and McKeegan K. D. 2008. A Vokrouhlicky D., and Gounelle M. 2010. Cometary origin refractory inclusion returned by Stardust from of the zodiacal cloud and carbonaceous micrometeorites, comet 81P ⁄ Wild 2. Meteoritics & Planetary Science implications for hot debris disks. The Astrophysical Journal 43:1861–1877. 713:816–836. Stadermann F. J. and Floss C. 2008. Abundance of presolar Niimi R., Kadono T., Arakawa M., Yasui M., Dohi K., grains in comet Wild 2 and implications for transport and Nakamura A.M., Iida Y., and Tsuchiyama A. 2011. In situ mixing in the solar nebula (abstract #1889). 39th Lunar and observation of penetration process in silica aerogel: Planetary Science Conference. CD-ROM. Deceleration mechanism of hard spherical projectiles. Stadermann F. J., Floss C., Gavinsky A., Kearsley A. T., and Icarus 211:986–992. Burchell M. J. 2009a. Calibrating the abundance Ogliore R. C., Huss G. R., Nagashima K., Butterworth A. L., determinations of presolar grains in Wild 2 cometary Gainsforth Z., Stodolna Z. J., Westphal A. J., Joswiak D., matter (abstract #1188). 40th Lunar and Planetary Science and Tyliszczak T. 2012. Incorporation of a late-forming Conference. CD-ROM. chondrule into Comet Wild 2. Astrophysical Journal Letters Stadermann F. J., Floss C., Kearsley A. T., and Burchell M. J. 745:L19. 2009b. Why are there so few presolar grains in samples Oliveira I., Olofsson J., Pontoppidan K. M., Van Dishoeck E. from comet Wild 2? Geochimica et Cosmochimica Acta F., Augereau J.-C., and Mern B. 2011. On the evolution of Supplement 73:1262. dust mineralogy, from protoplanetary disks to planetary Stodolna J., Jacob D., and Leroux H. 2010. Mineralogy of systems. The Astrophysical Journal 734:51. Stardust Track 80: Evidences for aqueous alteration and Poteet C. A., Megeath S. T., Watson D. M., Calvet N., igneous process (abstract #1657). 41st Lunar and Planetary Remming I. S., McClure M. K., Sargent B. A., Fischer W. Science Conference. CD-ROM. J., Furlan E., Allen L. E., Bjorkman J. E., Hartmann L., Takeuchi T. and Lin D. N. C. 2002. Radial flow of dust Muzerolle J., Tobin J. J., and Ali B. 2011. A Spitzer particles in accretion disks. The Astrophysical Journal infrared spectrograph detection of crystalline silicates in 581:1344–1355. a protostellar envelope. The Astrophysical Journal 733: Thomas N. 2009. The nuclei of Jupiter family comets: A critical L32. review of our present knowledge. Planetary and Space Price M. C., Kearsley A. T., Burchell M. J., Horz F., Borg J., Science 57:1106–1117. Bridges J. C., Cole M. J., Floss C., Graham G., Green S. Trigo-Rodrı´guez J. M., Dominguez G., Burchell M. J., Horz F., Hoppe P., Leroux H., Marhas K. K., Park N., Stroud F., and Llorca J. 2008. Bulbous tracks arising from R., Stadermann F. J., Telisch N., and Wozniakiewicz P. J. hypervelocity capture in aerogel. Meteoritics & Planetary 2010. Comet 81P ⁄ Wild 2: The size distribution of finer Science 43:75–86. (sub-10 lm) dust collected by the Stardust spacecraft. Tsuchiyama A., Mashio E., Imai Y., Noguchi T., Miura Y., Meteoritics & Planetary Science 45:1409–1428. Yano H., and Nakamura T. 2009. Strength measurement of Rietmeijer F. J. M. 2009. Stardust glass: Indigenous and carbonaceous chondrites and micrometeorites using micro modified comet Wild 2 particles. Meteoritics & Planetary compression testing machine. Meteoritics & Planetary Science 44:1707–1715. Science Supplement 72:5189. 470 D. Brownlee et al.

Van Boekel R., Min M., Leinert C., Waters L. B. F. M., Nakamura T., Naraoka H., Noguchi T., Okazaki R., Park Richichi A., Chesneau O., Dominik C., Jaffe W., Dutrey C., Sakamoto N., Seto Y., Takei M., Tsuchiyama A., A., Graser U., Henning T., de Jong J., Ko¨hler R., de Koter Uesugi M., Wakaki S., Yada T., Yamamoto K., A., Lopez B., Malbet F., Morel S., Paresce F., Perrin G., Yoshikawa M., and Zolensky M. E. 2011. Oxygen isotopic Preibisch T., Przygodda F., Scholler M., and Wittkowski compositions of asteroidal materials returned from Itokawa M. 2004. The building blocks of planets within the by the Hayabusa mission. Science 333:1116–1119. ‘‘terrestrial’’ region of protoplanetary disks. Nature Zanda B., Bourot-Denise M., Hewins R. H., Barrat J. A., and 432:479–482. Gattacceca J. 2010. The Paris CM chondrite yields new Walsh K. J., Morbidelli A., Raymond S. N., O’Brien D. P., and insights on the onset of parent body alteration (abstract Mandell A. M. 2011. A low mass for Mars from Jupiter’s #5312). Meteoritics & Planetary Science 45. early gas-driven migration. Nature 475:206–209. Zolensky M. E., Zega T. J., Yano H., Wirick S., Westphal Wickramasinghe J. T., Wickramasinghe N. C., and Wallis M. A. J., Weisberg M. K., Weber I., Warren J. L., Velbel K. 2009. Liquid water and organics in comets: Implications M. A., Tsuchiyama A., Tsou P., Toppani A., Tomioka for exobiology. International Journal of Astrobiology 8:281– N., Tomeoka K., Teslich N., Taheri M., Susini J., Stroud 290. R., Stephan T., Stadermann F. J., Snead C. J., Simon S. Wooden D., Desch S., Harker D., Gail H.-P., and Keller L. B., Simionovici A., See T. H., Robert F., Rietmeijer F. J. 2007. Comet grains and implications for heating and radial M., Rao W., Perronnet M. C., Papanastassiou D. A., mixing in the protoplanetary disk. In Protostars and planets Okudaira K., Ohsumi K., Ohnishi I., Nakamura- V, edited by Reipurth V. B., Jewitt D., and Keil K. Tucson, Messenger K., Nakamura T., Mostefaoui S., Mikouchi AZ: University of Arizona Press. pp. 815–833. T., Meibom A., Matrajt G., Marcus M. A., Leroux H., Wozniakiewicz P. J., Ishii H. A., Kearsley A. T., Burchell M. Lemelle L., Le L., Lanzirotti A., Langenhorst F., Krot J., Bradley J. P., Teslich N., and Cole M. J. 2010. A. N., Keller L. P., Kearsley A. T., Joswiak D., Jacob Survivability of Cometary Phyllosilicates in Stardust D., Ishii H., Harvey R., Hagiya K., Grossman L., Collections and Implications for the Nature of Comets Grossman J. N., Graham G. A., Gounelle M., Gillet P., (abstract #2357). 41st Lunar and Planetary Science Genge M. J., Flynn G., Ferroir T., Fallon S., Ebel D. S., Conference. CD-ROM. Dai Z. R., Cordier P., Clark B., Chi M., Butterworth A. Yurimoto H., Abe K., Abe M., Ebihara M., Fujimura A., L., Brownlee D. E., Bridges J. C., Brennan S., Brearley Hashiguchi M., Hashizume K., Ireland T. R., Itoh S., A., Bradley J. P., Bleuet P., Bland P. A., and Bastien R. Katayama J., Kato C., Kawaguchi J., Kawasaki N., 2006. Mineralogy and petrology of comet 81P ⁄ Wild 2 Kitajima F., Kobayashi S., Meike T., Mukai T., Nagao K., nucleus samples. Science 314:1735–1739.